Google
This is a digital copy of a book that was preserved for generations on Hbrary shelves before it was carefully scanned by Google as part of a project
to make the world's books discoverable online.
It has survived long enough for the copyright to expire and the book to enter the public domain. A public domain book is one that was never subject
to copyright or whose legal copyright term has expired. Whether a book is in the public domain may vary country to country. Public domain books
are our gateways to the past, representing a wealth of history, culture and knowledge that's often difficult to discover.
Marks, notations and other maiginalia present in the original volume will appear in this file - a reminder of this book's long journey from the
publisher to a library and finally to you.
Usage guidelines
Google is proud to partner with libraries to digitize public domain materials and make them widely accessible. Public domain books belong to the
public and we are merely their custodians. Nevertheless, this work is expensive, so in order to keep providing this resource, we liave taken steps to
prevent abuse by commercial parties, including placing technical restrictions on automated querying.
We also ask that you:
+ Make non-commercial use of the files We designed Google Book Search for use by individuals, and we request that you use these files for
personal, non-commercial purposes.
+ Refrain fivm automated querying Do not send automated queries of any sort to Google's system: If you are conducting research on machine
translation, optical character recognition or other areas where access to a large amount of text is helpful, please contact us. We encourage the
use of public domain materials for these purposes and may be able to help.
+ Maintain attributionTht GoogXt "watermark" you see on each file is essential for informing people about this project and helping them find
additional materials through Google Book Search. Please do not remove it.
+ Keep it legal Whatever your use, remember that you are responsible for ensuring that what you are doing is legal. Do not assume that just
because we believe a book is in the public domain for users in the United States, that the work is also in the public domain for users in other
countries. Whether a book is still in copyright varies from country to country, and we can't offer guidance on whether any specific use of
any specific book is allowed. Please do not assume that a book's appearance in Google Book Search means it can be used in any manner
anywhere in the world. Copyright infringement liabili^ can be quite severe.
About Google Book Search
Google's mission is to organize the world's information and to make it universally accessible and useful. Google Book Search helps readers
discover the world's books while helping authors and publishers reach new audiences. You can search through the full text of this book on the web
at|http : //books . google . com/|
:
I
i
. I
ANNUAL REPORT
OF
THE UNITED STATES
Geological and Geographical Survey
OP
THE TERRITORIES,
EMBRACING
COLORADO AND PARTS OF ADJACENT TERRITORIES;
BEING A
UPOKT or PK06RES8 OF THE EXPLORATION FOB THE YEAR 1874.
BY
F. V. HAYDEN,
UNITED STATES GEOLOGIST
GOKBUCTED UNDER THE AUTHORITY OF THE SECRETARY
OF THE INTERIOR.
WASHINGTON:
OOYBBNMBNT PBINTING OFFIOB.
1876.
//V
CONTENTS. /^//l/
Page.
Lbtfertothe Secretary 1
GEOLOGY, MINERALOGY, AND MINING INDUSTRY.
Report OF F. V. Hayden, United States geologist 19
Chapter I. Brief history of the Ligoitic group, first studied on the Upper
Missouri — early views entertained by Meek, Newberry, and other paleon-
tologists on the age of this group — the Lignitio group of the North-
west believed to be continuous southward with the Colorado and Lara-
mie beds 19
Chapter II. The Lignitic group as examined at Cafion City — Colorado
Springs — northward to Cache ^ la Poudre Creek — Monument Creek
group — ^probable age of tbese groups 28
Appendix to Chapter II, by H. T. West :J8
Chapter III. R^sum^ of the geology along the eastern base of the Front or
Colorado range : Silurian, Carboniferous, Triassic, Jurassic, and Creta-
ceous groups 40
The Carboniferous group 42
The Red beds or Triassic group 42
The Jurassic ^ 44
The Cretaceous 45
Chapter lY. Ancieut lake-basins — Glacial lakes — Moraiual deposits in the
valley of the Upper Arkansas River and along both flanks of the Sa-
watch Mountains 47
Chapter Y. General view of the geography and geology of the Elk Mount-
ains— eruptive granites — rhyolites and dikes — erosion on a grand scsde —
local drift-deposits 54
Chapter YI. Report on the Geology of the Northwestern portion of the Elk
range, by W. H. Holmes 59
Letter to Dr. Hayden 59
The Roaring Fork synclinal 59
Geology of bopris Peak and vicinity 61
Geology of the district drained by Rock Creek 63
The great fault-fold of the Elk range 68
Report op A. C. Peale, M. D.; geologist of middle division 73
Letter to Dr. F. V. Hayden 75
Introduction 77
Chapter I. Surface geology — valley of Eagle River 79
Chapter II. Surface geology — Grand River and its tributaries 85
Chapter III. Surface geology— Gunnison River and its tributaries 94
Chapter lY. Archoean areas of Ea^le, Grand, and Gunnison Rivers 106
Chapter Y. Stratigraphy — Paleozoic formations 110
Silurian age 110
Primordial period — Potsdam group 110
Canadian period — Calciferous and Quebec groups Ill
Remainder of Silurian 113
Devonian age 114
Carboniferous age 114
Permian or Permo-Carboniferous 117
Chapter YI. Stratigraphy — Mesozoio formations 121
Triassic \ 121
Jarassic 124
Cretaceous 128
Lower Cretaceous— Dakota group (No. 1) 128
Middle Cretaceous (No. 2 and No. 3) 135
Middle Cretaceous (No. 4) 137
Upper Cretaceous 137
III
I\r TABLE OF CONTENTS.
Page.
Report of A. 0. Pealk, M. D.— Continued.
Chapter VII. Stratigraphy — Cenozoic formations 140
Tertiarv .^. 140
Fort Union or Great Lignite group 141
Bear River group 144
Bitter Creek series 145
Wasatch group 147
Green River group 147
Wind River group 148
Bridger group 149
White River group 150
Lignitic group 152
Tertiary between Grand and Gunnison Rivers 156
Green River and Bridger groups 156
Post Tertiary and recent 161
Chapter VIII. Eruptive rocks — trachytes^trachorheites — basalt 163
Porphyritic trachytes 163
Trachorheites 168
Basaltic areas 171
Chapter IX. Economical geology ., 175
Catalogue of minerals 178
Catalogue of rocks 179
Report OF F.M. Emdlich, S. N. D 181
Letter to Dr. F. V. Hayden 183
Introduction : 185
I Chapter I. Metamorphic area 187
Chapter II. Yolcauic area 193
Chapter III. Sedimentary area 210
Silurian 210
Devonian 211
Carboniferous 214
Cretaceous • 221
Cretaceous (No. 1) 222
Cretaceous (No. 2) 224
Chapter IV. Mines 229
Occurrence of lodes 232
Highland Mary 233
The Robert Bruce * 2;?4
TheComstock lode 234
The Yreteva 234
Green Mountain lode 234
The Pride of the West 234
The Little Giant 235
Excelsior lode 235
The Prospector 236
The Pelican lode 236
BigCasioo 236
Ouray 236
Conclusion 239
Report of Samuel Augiiey, Ph. D 241
The superficial deposits of Nebraska 243
The Drift 243
The Loess deposits 245
Fruit on the Loess deposits 249
Scenery of the Loess deposits 250
Origin of the Lacustrine deposits.... ^ 250
Length of the Loess age 253
Life of the Loess age 254
Alluvium 256
The sand-hills 259
Alkali lands 260
The bad lauds.'. 261
Fuel from the surface-deposits 262
Water-resources of Nebraska 263
Timber in modern geological times 265
Mollusks in the Lacustrine deposits 266
TABLE OF CONTENTS. Y
PALEONTOLOGY. Page.
Rspoirr OF Lko Lrsqurreux a71
Letter to Dr. Hayden 273
On the Tertiary flora of the North American Lignitic, considered as evi-
dence of the age of the formation - 275
Table of anbdivisiona of the Tertiary of Europe, according to the floras 284
Table exposing the relation of the fossil plants of Point of Bocks 2»6
Description of species of fossil plants from Poi n t of Rocks 296
New species of Tertiary fossil plan ts briefly described 306
A review of the Cretaceous flora of North America - - - 316
$ 1. General remarks 316
$ 2. Description and enumeration of generic and specific divisions .... 333
ARCHEOLOGY.
Report of W. H, Jackson 367
Ancient ruins in Southwestern Colorado * 369
ZOOLOGY.
Report OF Ernest Inobrsoll 383
Natural history, 1874 385
Letter to Dr. F. V. Hayden 385
List of localities of specimens 386
General account of the work 387
Special report on the Mollusca : 389
List of authorities 407
I TOPOGRAPHY AND GEOGRAPHY.
Reports of Henry Gannett, S, B, Ladd, and A. D, Wil9on.
Report OF Henry Gannett, M. E 413
Introductory letter 413
Chapter I -• 415
' Previous explorations in the district 415
Geography of the district 416
Height of the walls of the Grand Cation of the Gunnison 426
Distribution of vegetation '. 428
Settlements, trails, roads, etc 428
; Chapter IL Elevations 429
Revision of the heights of summits in the Sa watch and Elk systems.. . 429
Elk Mountains 430
On the plateau 432
Report of S. B. Ladd, M. E., northern division 435
Letter to Dr. F. V. Hayden 435
Report 435
Roads and trails 439
List of elevations 441
Report OF A. D. Wii^ox 443
Means of communication between Denver and the San Juan mines 443
Comparisons of aneroids with the mercurial barometer 447
Report OF Franklin Rhoda ,.., 451
Topography of the San Juan country 451
Ascent of Mount Sneffels 479
Methods used in determining the elevation of points in the district 488
Notes useful for the location of miners' monuments in Baker's Park 496
General index 497
Systematic indrx 509
LIST OF NEW SPECIES DESCRIBED.
FOSSIL PLANTS.
FocQB lignitnm 296
Balvioia attenuata 296
fielagmellaf falcata 297
laciniata 297
Seqnoia biformis 298
I
I
VI TABLE OF CONTENTS.
Fage.
Widdriugtonia complanata 299
Pistia corrngata , 299
OtheliaAruericana 300
Dryophyllam crenatam 301
subfalcatam - 301
Popalns melanaroides ■ 302
Trapa microphj'Ua 304
Lauras (Persea) prtesteDS f 305
Viburnum rotundifolium 305
Greviopais Clebumi 306
Rhus membranacea 306
Alnites uneqnilateralis 307
Juglans alkalina 308
Carpites viburni 308
Spheria rby tiBmoides liOS
Uypnum Haydenii 309
Lygodium Marvinei 309
Dentooi 309
Zamiostrobus ? luirabilis 309
Sequoia atflaiH 310
acuminata 310
Arundo reperta 311
obtusa 311
Palmacltes Goldianus 311
Sabal communis 311
Myrica insignis 312
TLessigiana 312
Betula Vogdesii 312
Castanea intermedia 313
Ficnsovalis 313
Ficus pseudo-populus 313
Wyomingiana 314
Diospyrost licoidea , 314
Viburnum platanoides 314
Cissus parottiiefolia 314
Leguminosites alternans 31?>
Sapindus Dentoni 3ir>
Lomatia microphylla • 3ir>
Sequoia condi la 335
Myrica cretacea 3:^9
Dryopbyllum (Quercua) latifolium 340
salicifolium 'MO
Ficus lauropbyllum 34^
distorta 342
Laurus protesefolia 343
Daphnogene cretacea 343
Andromeda affinis 348
Aralia tripartita 348
concreta 349
Towneri 349
Saportanea ' 350
Hedera Schim]>eri 351
platanoidea 351
Cissitee acnminatus 353
Heerii 35.'^
Ampelopbyllum attenuatum 354
Menispermites ovalis 357
cyclophylluB 368
Steroulia lineariloba •. 358
Ilex strangulata 359
Protopbyllum crednerioides 36.3
MOLLU8CA.
Pnpilli alticola 391
Limax montanus :I94
castaneus 396
Helix (Micropbysa) Ingersollii 397
Helisoma plexata 402
TABLE OF CONTENTS. VII
LIST OF ILLUSTRATIONS.
Report of F. V. Haydmn.
Kow Faclog'pftg^—
1. Plato L SLowing variability of the Lignitic beds 30
^ } Section at Bear Creek ( '*'*
3. Plate II. \ l\«' I' ^*^^® .^'^Vl! "^^P^ ^'^^ trachyte . . > 34
^ Fig. 2. Deposit of lignite m an irregalar cavity in sandstone .. 5
4. Plat«III. Monnment Park, Colorado 36
•'>. Geological map of Colorado Springs and vicinity 40
6. Sections accompanying map of Colorado Springs and vicinity 40
7. Preliminary map of eastern base of Rocky Mountains 41
8 Plate IV ) ^^^' ^' ^^^^^ Rock in Glen Eyrie, Triassio sandstone ) ^l
* ^ Fig. 2. Concretions of sandstones, Cretaceous period i
9 Plate V i ^^^^' ^* Showing changes in sediments / ^«
i Fig. 2. Thickening of sedimentary beds near Manitou >
C Fig. 1. Cross-bedding, Lignitic sandstones, near Colorado Springs )
10. Plate VI. -^ Fig. 2. Silarian limestones resting nnoooformably on stratiti^ > 44
( granite, William's Cafion )
11. Plate VII. Surface-section near Glen Eyrie, Colorado 42
12. Plate Vin. Gateway to the Garden of the Gods 42
13. Plate IX. Cathedral Rock, Garden of the Gods 43
14. Pleasant Park, from the south 44
15. Plate X. Foliation of granite in Estes Park, Colorado 46
16. Plate XI. Long's Peak and Estes Park, Colorado 46
I* 5 Sketch and sections showing the moraines of the Upper Arkansas Valley > .q
*'• ) inColorado 5 *®
1^. Moraines of the Upper Arkansas 49
19. Plate XII. Boulder Cafion, Colorado, granite 50
20. Plate XIIL Chicago Lake, Colorado 52
21. Plate XVI. A portion of the east face of Gothic Mountain 54
22. Plate XV. Mountain of the Holy Cross, Colorado 54
Report of W. H. Holmes. •
23. Fig. 1. Sections across the synclinal valley of Roaring Fork 60
2* J Fig. 2. Chart of Sopris Peak ) go
• I Fig. 3. Section across the Sopris uplift )
25). Fig. 4. Sketch looking down Rock Creek 63
26. Fig.5. Geolojp' of station 23 64
27. Fig. 6. View ill the Snow Mass group ., 65
28. Fig. 7. Treasury Mountain 66
29. Fig. 8. Cascades on Rock Creek 67
30. Fig. 9. Relations of the coal-beds to No. 1 Cretaceous 69
31. Fig. 10. Sections across fault-fold of Elk Mountains ^n^4-«,««« -rn o«i^ -ri
32. Fig. 11. Part of the great fault-fold of Elk Mountains ? between 7U ana 71
3;i. Map of the Elk Mountains, Colorado / nz>*«r^«« to ^r^A yt
U, Sections accompanying map of Elk Mountains J between 7Z ana 7d
Report of A. C. Peale.
33. Sheet of conventional s^gns 76
SFig. 1. Section A. South from Eagle River )
Fig. 2. Section B. Across Eagle River to Holy Cross Mount- > 80
SFig. 1. Secti<
Fig. 2. Secti(
ain .
37. Plate IL Fold on Eagle River 82
•« PUfA TTT 5 ^^^J?' '• Section C. Across Eagle River to station 9 ) on
«. riate 111. ^ pj^ g Section D. Eagle River to station 9 J ^
39. Map A. Showinglinesof section on Eagle River 84
Mi Pi«+^TTT 5 ^^*S* 1* S^^^*<>" *^' Across Grand River ) qh
w. riate i\ . ^ pj^ 2. Section F. From station 13 to station 14 } ^
41. Plate V. Bluffon Plateau Creek 91
4*2. Plate VI. Bluff on Grand River near the mouth of the Gunnison 92
n xi\ 4- XTTT S ^^^S' ^' Section G. From station 38 to Gunnison River I ^y.
4i I'late VII. J pjg 2. Section H. From station 77 to Cedar Creek 5 ^
44. Map B. Showing lines of section across Gunnison River 100
f Fig. 1. Section I. From Gunnison River westward ^
i.^ m « xriTj ) FifiT* ^- Section K. Across the Gunnison below North Fork ..I ^f^
«). riate V 111. < p^^ 3 gection L. Across angle of Gunnison below the Grand f *"^
Cafkon .—.J
VIII
TABLE OP CONTENTS.
46. Plate IX
{ Fig. 1.
. ^Fig.2.
I Fig. 3.
I7o. Facing
Fig. 1. Section across monoclioal fold soath of Grand River..
Section across monoclinal fold west of Gnnnison River
Section M. From Gunnison River east to mesa
47. Plate X. Bluflf at head of Oli-be-joyful Creek
48. Plate XI. Bluff on Coal Creek
49. Plate XII. Dikes in sandstone on Anthracite Creek
50. Plate XIII. Dikes in bluff at head of Oh-be-joyful Creek
51. MapC. Showing areas of por))hyritic trachyte
52. Plate XIV. 1 1!!|; J*
I Fig! 4.'
53. Map D. Showing areas of trachorbeites and lines of sections across the Gnn-
nison River
54. Map E. Showing basaltic areas between Grand and Gunnison Rivers and line
of section M •
Sections across Gunnison River above Grand Cafion
poge-
105
138
la^
164
165
166
169
170
174
Rbport of F. M. Endlich.
55. Fig. 1. Monuments near camp 23, east of station 10 ^ 195
56. Fig.2. Lizard'sHead ..' 207
57. Section I. From station 48 through station 49 214
58. Section II. From station 31 toward Sultan Mountain 217
59. Section III. Through station 37 218
60. SeotionlV 219
61. Section V. A«station40 283
62. Section VI. Through station 47 ^4
63. Section VII 2l6
64. Section VIII 227
65. Fig. 3. Metalliferous veins near Ho wardville, Colo 232
Report op Samuel Aughby.
66. Arrows found in the Loess (wood-cut in text) « 255
67. Plate I.
68. Plate II.
69. Plate III.
70. Plate IV.
71. Plate V.
Report of Leo Lesqubreux.
Fig. 1. Aralia tripartita
Figs. 2, 2*. Aralia Saportanea
Figs. 1, 2. Aspidiophyllum trilobatum
Fig. 3. Ampelophyllum attenuatum
Fig. 4. Phyllocladns subintegrifolius
Figs. 5, 5*. Gleichenia Nordeuski51di
Fig. 1. Protophyllum crednerioides
Figs. 2; 8, 8^ Sequoia fastigiata
Fig. 3. Hedera platanoidea
Fig. 4. Myrica cretacea \
Fig. 5. Andromeda affiuis
Figs. 6, 6», 7, 7*. Pinus Quenstedti ffeer
Fig. 1. Aralia Towneri
Figs. 2, 4. Aralia concreta
Figs. 6, 7. Sequoia condita V
Fig. 8. loolepis ? apeaea
Fig. 9. Prunnsf cretacea Lesqx..
Figs. 1, 2. Laurus prqte»folia
Fig. 3. Menispermites populifolins
Fig. 4. Menispermites ovalis
Fig. 5. Ficus distorta
Fig. 6. Protophyllum minus
Fig. 7. Ficus laurophyllum
366
366
366
366
366
72. Plate VL
73. Plate VIL
fFig. 1. Dryophyllum (Quercus) latifolium
{ Fig. 2. Lomatia Saportanea Lea^
Fig. 3. Cissites Heerii
.Fig. 4. Menispermites eyclophyllus
Figs. 1, 2. Cissites Harkerianus Lesqat . .
Fig. 3. Menispermites obtnsilobaXesfx.
Fig^ 4. HamamelitesEansaseanaLe^gx.
Fig. 5. Hedera Schimperi
366
Job
TABLE OP CONTENTS.
IX
Ko.
Facing page—
j Fig. 2. Drvopbyllam (Qaercns) salicifolium
74. Plate VIII. < Fig. 3. Ilex straDffulata
I Fig. 4. ProtophylTum credDerioides
i^Fig. 5. Platanas Heerii
I
366
76. Plate II. i
Report of W. H. Jackson.
Fig. 1. Gronnd-plan of roand tower on the Rio Mancos
Figs. 2, 3. Tower adjoining a rectangular foundation in the
cafion of the Mancos.
75. Plate I. \ Fig. 4. A portion of doorway and one comer of a oarefully-
Duilt house, Mancos Cation.
Fig. 5. Cliff-house on the rocks of Mancos Ca&on
Fig. 6. Inscriptions on cafion-walls
Fig. 7. Cliff-house in Mancos Cafion
Fig. 8. Showing the tenacity of cemen ting-material
Fig. 9. A square tower in the valley of the MoElmo
Fig. 10. An isolated rock in the valley of the McElmo covered
with ruined houses and walls.
Fig. 11. Ground-plan of an extended series of houses in the
valley of the Hovenweep.
'Fig. 12. A two-story house in the crevices of the escarpment
in the Mancos Canon.
1 Fi^. 13. A general view of the valley of the Rio Mancos near
I its outlet from the Mesa Verde.
^ I Fig. 14. A view of ruined village in the valley of the Hoven-
t weep. '
rV. Cliff-house in the cafion of the Mancos.....
V. Battle-rock in the cafion of the McElmo
VI. Cave-dwellings in the cafion of the McElmo
VII. Watch-tower in the cafion of the McElmo
VIII. Ruins in the cafion of the Hovenweep, Utah
369
370
77. Plate UI.
k
Plate
79. Plate
80. Plate
81. Plate
82. Plate
370
372
374
376
378
380
Report of Ernest Inoersoll.
83. Pupilla alticola (wood-out in text) 392
84. Limax montanus (wood-cut in text) 394
85. Lin^raal dentition of Limax castaneus (wood-cut in text) 396
86. Helix (Microphysa) Ingersollii (wood-cut in text) 398
87. HeUoeoma plexata (w<x>d-cnt in text) 402
Reports of Henry Gannett, S. B. Ladd, and A. D. Wilson.
88. Preliminary map of Central Colorado 412
LETTER TO THE SECRETARY.
Oppiob United States Geological and
OEOaBAPHIOAL SUBVEY OF THE TEBBITOBIBS,
Washingtonj D. C, October 1, 1876.
Sib : I have the honor to present for pablication the Annual Report of
the United States Geological and Geographical Survey of the Territories,
embracing a pi-eliminary accoant of its operations in portions of Colo-
rado daring the season of 1874.
The headquarters of the survey in the field were made at Denver, as
in the preceding year, as the most suitable point for procuring the outfit
and making the necessary preparations for the various divisions which
were to investigate the districts specially assigned to them by the geol-
o^st-in-charge. The entire survey was separated into seven divisions.
Pour were for regular topographical and geological daty, and were
assigned to specific areas; one party for the primary triangulation ; a
photographic division, to which was attached a naturalist ; a party for
special topographical and geological study ; and the quartermaster's
division, that furnished all the parties above mentioned with supplies
during their field-work.
The first division was composed as follows: — A. B. Marvine, assistant
geologist, director; S. B. Ladd, topographer; Louis Chauvenet, assistant
topographer ; M. L. Ward and W. S. Holman, meteorological observers;
E. A. Barber, botanist and collector; W. W. Williams, general assistant;
together with two packers, cook, and hunter.
The party took the field on the 20th of July, crossing over Berthoud's
Pass, and through the Middle Park into the North Park, by the Willow
Creek Pass. The survey of the southern portion of this park employed
the party for some time; and it was not until the middle of August that
they crossed to the main field of their work west of the Park range.
This new area presented all the different forms surface-erosion peculiar
to a granite, sedimentary, and lava country, making it an exceedingly
interesting study both for its topography and geology. The great
lava mesa situated at the head of the White Biver is cut by deep cations
that penetrate far into the plateau, dividing the mesa into what appear
to be isolated masses, but which are all connected. One isthmus, from
three to twelve feet in width' and one hundred and twenty-five in
leDgtb, connected a plateau, of several miles extent, with the main
mesa. The highest portion of this mass is on the east side, and, from
the base of the almost continuous cliffs which border it, the country
descends in long, timbered slopes to the broad, open area of Egeria
1 H
2 GEOLOGICAL SUEVEY OP THE TERRITORIES.
Park, lying between them and the Park range. Portions of this park
drain into the Grand, but the greater part into the Bear, the divide
between the two being very low.
The old Salt Lake wagon-road enters here from Gore'8 Pass. The
top of the plateaa is a rolling bountry, with numerous isolated mount-
ain-masses. It abounds with numerous small lakes, and is well tim-
bered, chiefly with fine spruce. To the west, the plateau gradually falls,
the lava top dies out, the sedimentary rocks appear on the surface, and
the timber-growth changes to aspen and pine.
The valley of the Grand does not present the attractive agricultural
features of the White and Bear Rivers. It has formed numerous canons,
which show in a very interesting manner the highly-colored rocks,
bent and twisted by many folds. Dwarf cedars, juniper, and the finer
pines cover the slopes for some distance up, and the ever occurring sage-
brush the flat bottom-slopes. South of the Grand, and between that
and the Eagle, the country rises in broken, irregular mountain-ridges to
the rough snowy range, of which Mount Powell is the culminating
point.
Going west of the plateau, the rain-fall becomes continually less until
the party reached 108^, when it entered upon the dry, barren country
of Western Colorado. Snow fell in considerable quantities early in Octo-
ber, and the clouds that hung around the topographical points caused a
great deal of delay. The weather finally grew so bad that it was decided
to work toward civilization. An attempt to reach the White River
Indian agency by a trail across the mesa was frustrated by the snow.
The party reached the top in a blinding snow-storm, with snow nearly
two feet deep. One of the party, who had crossed with the mail two weeks
before, reported the snow as belly-deep to a horse for fifteen miles, aud
in places for a considerable distance up to the top of the saddle. After
one night's camp in the snow, and the storm still continuing, the party
decided to turn back, and take the longer but easier route around the
mesa. This route ofiered no difficulties, and they finally reached Raw-
lins Springs, the nearest point on the Union Pacific Railroad, Novem-
ber 27.
A barometric station was established at the agency, and one of the
meteorological observers was there all the time. This station will serve
as the base for all altitudes in the district. In October, this party
divided, a portion remaining encampedatthe mouth of the Eagle, where
icareful barometric readings were taken that will fix this important point.
.Approximate determinations of the amount of water in the Eagle,
Grand, and Bear Rivers were made, which will give an idea of the
amount available for irrigation.
The amount surveyed is about forty-three hundred square miles, com-
prising a narrow strip of country, taking in the south side of North Park,
stretching from Long's Peak to the Park range. The main portion is
bordered by the Park range on the east, south by the Eagle and Grand
LETTER TO THE SECRETARY. 3
Rivers, and north by the Bear Eiver. Westward 'the work extends
nearly to longitade 108^.
The operations of this division during the field-season of 1874 were
directed, first, to the survey of a narrow east and west strip along tbe
southern edgeof the North Park, thus extending the work of the previous
season in the Middle Park northward to the parallel of 40° 30' north lati-
tude; and, secondly, the extension of the same work westward over the
Park range and along the region of the Bear, White, and Grand Rivers,
this being the principal field of work. Here, the northern boundary of the
survey, 40^30', is practically the Bear River; while the southern boun-
dary was formed by the Eagle River to its junction with the Grand, and
below thispoint by thelatterriver itself; ontheeastthe Park range, about
in longitude lOG*^ 3(y, limited the arfea in question ; while to the west the
survey was carried to an irregular border, about touching, at its extreme
point, the meridian of 108o. The narrow strip in the North Park prob-
ably covers over five hundfed square miles, while the principal and more
compact area at the west may be considered as averaging nearly seventy
miles across east and west and nearly sixty miles north and south, or about
four thousand square miles in area. Topographicall^'^, this area may be
dinded into three well-marked divisions: first, the region draining mostly
northward into the Bear; secondly, that draining southward into the
Graud and Eagle Rivers; and, thirdly, the basin of White River and its
tributaries, which in itself forms a .complete drainage-system, trend-
ing westward directly be^ween the two preceding regions. At its source,
the Bear, with tributaries of the Grand, quits the sources otHhe White,
which rise in a great isolated mesa-mass of lava, between which and the
Park range is the deposited basin of Egeria Park.
The whole region was examined in the usual manner of the survey:
first, such observations were made as to enable a carefully-colored geo-
logical map to be constructed, showing the distribution and extent of
the rocks, and formations of varions ages or kinds, which compose the
surface of the region ; sections numerous enough to show how these
various formations lie upon one another, or how they probably lie beneath
the visible surface, or to show the various foldings or fractures to whidh
they have been subjected and yielded ; and as many detail-sections as
possible, to determine the changes which take place in the character and
thickness of these formations in their lateral extension, and to deter-
mine, as closely as possiblo^ their relative ages and general paleontolog-
ical relations. In this connection, the extent and mode of occurrence of
all economical products, as minerals, building-stones, plasters, springs,
etc, are noted as far as observed, while collections of specimens of the
same, as well as of all rocks, fossils, etc., are made as far as possible.
Second, and chiefly to enable some of this knowledge to be more accu-
rately represented, such operations are carried on as to enable a
map, or representation, of all the surface-features of the country to be
prepared, its rivulets, streams, plains, hills, and mountains, its canons
4 GEOLOGICAL SUBVET OF THE TEBRITOBIES.
or valleys, its steeper or greater slopes, its peaks and passes, and this
with all the accaraey that it is possible to give on a map printed on a
scale of four miles to an inch, and in 200-foot contour-lines. These
topographical observations are directly fonnded on a careful secondary
triangnlation, carried on simultaneoueJy with them. At the principal
stations of this triangnlation, stone monaments from four to six or more
feet in height were built, with a wooden stick, on which was deeply
carved the number of the station and of the map (according to the
scheme of maps of the survey), inserted in each, thus rendering
them available in the future, when more accurately located by the pri-
mary triangnlation, as dat.a on which to base the usual United States
land surveys when these may be needed in these distant regions, or for
other purposes of references.
Further, the general quality and distribution of timber, bottom, agri-
cultural, arid, or generally unavailable lands, were also made the sub-
ject of observation ; while botanical, natural-history, and other speci-
mens were collected as far as possible; and the amount of water flowing
in the larger streams was made, in some cases, the subject of measure-
ment. A permanent and quite complete meteorological station was
established at the White Biver agency, the base of supplies of the party,
while similar observations were at one time continuously taken for
nearly three weeks at a point near the head of the White Biver, and
again for nearly four weeks at the junction of the Eagle and Grand. In
comparing with thcMe bases the observations constantly made with the
party, very complete and accurate hypsometric results will be obtained.
In these observations, the usual mercurial mountain-barometer of James
Green, with wet, dry, maxima, and minima thermometers, was employed.
As the general results, regarding the occurrence of economic products,
it may be said that the series of older metamorphic rocks, such as the
granites, schists, etc., of probable Archean age, in which alone the
precious metals and minerals of Colorado have been found, and which,
form the foundations on which all the bedded rocks, sandstones, lime,
stones, etc., of the country rest, are brough: to the surface and exposed
only along the folded ridges of the Park range, and in the bottoms of a
few caiions in some of the southern tributaries of White Biver, and of
the neighboring tributaries of the Grand, and that it is only in these
regions, therefore, that, the precions minerals may be looked for. Along
the northern portion of the district, north of the main valley of the
White, and in the extreme west, the surlace*of the country is formed of
rocks of .Cretaceous age, which are, for the most part, horizontal beds,
flexed here and there into quiet undulations. The coal of the region,
which consists of a few seams of fair Lignitic coal, seems to be confined
wholly to pretty definite horizons in the upper-middle and upper por-
tions of this group ; and as these particular horizons have been eroded
away from the region in question, except at the north and west, it is here
alone that it becomes worth while to search for coal. Farther west, it is
LETTER TO THE SEGBETAB^. 5
anderstood tbat both in qaantity and quality, this coal improvea. In
the sontheastcra portion of the district, above the Grand and Eagle
Bivers, the sedimentary rocks, from the extreme base of the Cretaceous
down to the granite rocks of the Park range, occar, all thrown iuto a
series of complicated and pecoliar folds. Limestone occurs near the
Grand in abundance, and on both the Grand and Eagle Bivers are grea4;
deposits of gypsum, though other economic products, except some salt
SDd soda springs, will probably not be found here.
The imposing mesa about the head of White River and several larger
areas near the Park range are composed of great floods of volcanic
rock, which have poured over the country in comparatively rocent tiroes,
but some of which are yet old enough to have experienced the vicissi-
tudes of the Glacial period 6f the West, and to have received a profound
iojprees from erosion, similar to that now going on over the whole
country.
The topographical work of the party under my immediate direction
was intrusted to Mr. G. B. Chittenden, and was divided into three parts :
first, the mapping of the peculiar features of the morainal deposits in the
Upper Arkansas Valley; secondly, the reworking of the topography of the
Elk Mountains on a larger scale, and with more detail than was possible
daring the preceding season in the regulfir progress of the survey ; and,
finally, the laying down of the topography, and the line of junction of
the metamorphic and sedimentary rocks, and also the coal-outcrops on
the eastern base of the mountains, from Canon City to the northern
lioundary of the Territory, making, in this latter division, small detailed
maps where points of particular interest or peculiar complication made
them seem desirable. In pursuance of this plan, the work began at
Colorado Springs, in order to investigate that region in detail, liefore
the main party would be ready to proceed across the South Park to the
work in the west. Forty-five topographical stations were made on the
sedimentary rocks, within ten miles of the springs, embracing the Gar-
den of the Gods and Monument Park, so curious on account of their
geological stmctore, and well worth mapping as typical geological fea-
tures, which might be readily reached by the student traveling from the
east Joining the main party here, we crossed the South Park to the
Arkansas Valley, carrying on a running survey of*t be road as we traveled.
By short marches for five days up the valley, we were euabled to study
out, with a good degree of care, the heavy masses of morainal deposits,
which, for twenty miles or more, sweep out from the base of the high
mountains which border^ the valley on the west to the present channel
of the river. It will, of course, be impossible, in the time devoted to
these moraines, to make a carefully-detailed map of them, but enough
notes were taken to give quite accurately their relations to each
other, their general forms and magnitudes, and their particular trends,
together with their relations to the surrounding mountains.
Ijeaving this region about the middle of August, we crossed the main
divide by way of the Lake Creek Pass and entered the Elk Mountains.
6 GEOLOGICAL SURVEY OF THE TERRITORIES.
This range reaches out from near the headwaters of the Gannison
River, i'orty miles to the northwest, and, though not generally as high as
the olher ranges of Northern Colorado, is by far the most rugged of them
all. The reasons for re-examining this range, when it had been sur-
veyed in the regular progress of the work, were two : first, their rug-
gednessand inacoessibility had made the difficulty of .working them last
year so great, that they were not surveyed in a style quite up to the
standard of fihe remainder of the work ; and, secondly,, that their geo-
logical importance made it a matter of particular scientific interest that
they should be carefully studied and mapped.
The geologist and. topographer worked side by side through them,
making forty-two high mountain-stations; Mr. Holmes sketching the
different portions of the whole mass from as many points as possible.
They contain about eight hundred square miles, and will be mapped on
a scale of one mile to the inch.
Marching from here by way of the Twin Lakes and South Park to
Cafion City, we carried on a running survey along our route, and from
the latter place commenced work, on the last part of the summer's plan,
the mapping of the sedimentary border-line and that of the coal from here
to the Wyoming line. This work, carried on without interruption, was
finished by Mr. Chittenden, Mr. Holmes, and myself on the 20tb of
October ; it having required seventy-four topographical stations. This
survey was of a great deal of practical as well as scientific importance, and
of immediate need, since, in the coal-series, we wereenabled to lay down
pretty closely that broken winding line more than two hundred miles in
length inside of which no coal might be found. The labor involved in
carefully laying down this line cannot be realized until one notices the
almost numberless prosi)ect-holes that hare been sunk into the worth-
less black shales which, all along the base of the mountains, lie inside
the coal-series and tempt the settlers into profitless investments and
unrequited diggings after coal.
In carrying on this last survey, the Land-Office work has been of
great assistance, and also the careful studies of Captain Berthoud of
the coal lying to the west and north of Denver.
The maps produced from this special survey and included in this
report are as follows : —
1. A map of the eastern base of the mountains from below the Arkansas
Biver to the northern line of the Territory, on a scale of two miles to
one inch. On this map are plotted the line of coal-outcrop, the junction
of the sedimentary and metamorphic rocks, and the inner limits of the
Cretaceous.
2. A map of the Elk Mountains on a scale of one mile to an inch, plot-
ted with 200-foot contours.*
3. A map of the Upper Arkansas Valley^ showing the heavy morainal
deposits in the vicinity of the Twin Lakes, on a scale of one mile to an
inch.
*Theee maps are all redaced one-half for publication.
LETTEB TO THE SECRETARY. 7
4. A map in the vicinity of Colorado Springs^ on a scale of one-half a
mile to an iDch, made principally' for geological purposes.
The meanders of traveled roads will be plotted on the final maps of
Colorado.
While all this work was looked upon as special work, and done with
more detail than the regnlar work of the survey, the results will, of
course, be incorporated in the final maps of the Territory, and form a
part of them.
During the season, Mr. Chittenden made 156 topographical stations,
and the total area surveyed was over four thousand square miles. Mr.
W. H. Holmes labored with his usual zeal and skill during the entire
season, and much of the accuracy and value of the work is due to him.
During the sickness of ^ member of the party at the base of Sopris
Peak, I was detained about twenty days. In the mean time, Messrs.
Holmes and Chittenden made a careful geological and topographical
study of the northwestern portion of the Elk Mountains, the results of
Which will be found embodied in Mr. Holmes's report. Great numbers
of topographical and geological sketches were made by Mr. Holmes,
which will serve in a remarkably clear manner to illustrate the
structure of the interesting regions surveyed.
The district assigned to the second division is limited on the north by
the Eagle and Grand Eivers, west by the west line of Colorado, south
by the parallel of latitude 38° 20', and east by the 107th meridian. The
area of this district is about seven thousand square miles, of which the
party completed 5,300 square miles.
The plan of the geodetic and topographical work is as follows:
1st. The latitude and longitude of certain points are determined by as-
tronomical observations as accurately as the present state of astronomical
science will allow. This work has been done for us, thus far, by the
United States Coast Survey. For the prosecution of the survey of Colo-
rado, the latitude and longitude of Sherman and Cheyenne, Wyoming
Territory, and Denver, Colorado Springs, and Trinidad, Colorado Terri-
tory, have been determined by them.
2d. From a base-line measured as accurately as possible, a system of
primary triangulation is expanded and extended to cover the area to be
surveyed with a net- work of triangles* By this operation, the positions
of a limited number of points are established with accuracy. Connect-
ing this system of triangulation with the points whose positions have
been established by astronomical observation, the latitudes and longi-
tudes of the primary points are established. Ihe first base-line for the
primary triangulation of Colorado was measured principally on the
track of the Kansas Pacific Bailroad near Denver. Its length is between
six and seven miles. Check-bases at Colorado Springs and in San Luis
Valley have also been measured and connected with the triangulation.
The angles are measured by a 15-inch theodolite, reading to ten
seconds, using artificial signals. The primary triangulation is carried.
8 GEOLOGICAL fiURYET OF THE TERBITOBIES.
on by a special party. Using the lines of the primary system as bases,
the topographers of the division carry on the secondary triangulation,
locating points within the triangles of the primary system. In the
secondary system, as in the primary, all three angles of the triangles are
measured, and, in most cases, artificial signals are nsed on the stations.
The instrament nsed for this work is a sort of theodolite, reading
minates. The stations for triangulation and topography are, in most
cases, the highest and most commanding points, and are so selected that
the limits of work from one will reach the limits from those aronud it.
From a station, a sketch-map of all the country within the range of vision
is made, as also a prospective sketch. Angles taken on prominent points
and recorded on these sketches serve to locate them, and thus to correct
the sketch-map. The distance between stations must depend on the
character of the country, but the average distance apart is seven to ten
miles. For the prosecution of its work during the past season, this
division made eighty-six stations, or one station to every eight miles of
area.
The most prominent geographical features occupied by this division
are in brief as follows : On the north, the Eagle or Piney Jiiver flows,
through most of its course, in a broad fine valley, having a course nearly
west, interrupted here and there by short carLons. At its mouth, it is a
large stream, barely fordable at the lowest stage of water. The Grand
Biver, sometimes called the Blue or Bunkara, below the mouth of the
Eagle, is in a close canon about thirty miles, interrupted by a short
meadow at the mouth of Bearing Fork. Below this canon, the river
flows sluggishly through a broad meadow, which extends for fully fifty
miles, but is narrowed in the middle of its length, where the river cuts
through a plateau. Below this meadow, the river enters another canon
about eighteen miles in length, and of no great height, from which it
flows into the broad valley in which it meets the Gunnison. The course
of the Grand, at the month of the Eagle, is about west, which direction
gradually changes to southwest, and then near the mouth of the Gun-
nison again to the west.
The drainage of the southern part of the district is by the Gunnison
Biver. This stream takes all the water from the southern slopes of the
Elk Mountains, the western slopes of the Saguache range, and the
northern slopes of the Uncompahgre Mountains. For twenty-five miles
below the month of Oochetq[>a Greek, this river is in a narrow valley,
which is diversified by long tongues of mesa, which separate the
numerous streams entering the river on either side. Below this valley
is a very heavy caiion cut in a high plateau for fifteen miles. The
plateau is horizontal, 10,0<K) feet high, and the course of the river is
nearly west across it, the depth of the caiion increasing with the fall of
the river from 3,000 to 4,000 feet. At this point, the plateau breaks off
abruptly on the north side, and, while preserving nearly the same height
at the edge of the caiion, slopes off gradually toward the north, having
LETTER TO THE 8ECBETAST. 9
the appearance of long bog-backs. On the south side, the plateau pre-
serves its horizoutality for a few miles, then breaks off, leaving a ridge
of uptarned beds only to separate the river from the valley of the
UDcoiupahgre. At a point about thirty miles below the head of the
canoD, the river changes its course abruptly from west to north, and
flows parallel to the slope of long hogbacks, it holds this coarse for
aboQt eighteen miles, then, at the mouth of the Nprth Fork, a large
affluent from the north, it tarns again abruptly to the west, and a few
miles farther suddenly emerges from the cunon into the broad valley of the
Uocompahgre. The character of this cafion in its api)er part is extremely
ragged ; its walls are precipitoas, and there is hardly a place where a
man could clamber down to the bottom. The river fills the bottom of
the caiion, leaving no beach anywhere. The material of the caiiou-
walls in the upper two-thirds is gneiss and in the lower third stratified
rock. The valley of the Uncompahgre Biver is very broad, extending
forty miles up the Uncompahgre Biver and twenty miles down the
Gunnison. Below this, the river falls throngh a canon, which, with
slight interruptions, extends to the mouth of the river, while the country
back from the river is a flat open valley.
The Elk Mountains extend into this district, occupying an area of
about one thousand five hundred square miles in' the southwestern
part Their character is not that of a continuous range, but of groups
of mountains and isolated peaks. The elevation of the highest does not
exceed 13,500 feet, and the average of the peaks is scarcely 13,000 feet.
These mountains are drained entirely by the Gunnison ; the northern
slopes by its North Fork. Besides these mountains, the country is
entirely plateau and broad valleys. The plateau has an elevation of
8,500 to 10,000 feet, sloping gradually toward the west. The elevation
of the mouth of the Gunnison Biver is about j4,200 feet ; at the mouth
of the Uncompahgre, 4^500 ; and the general elevation of the Uncom-
pahgre Valley, 4,500 to 5,000 feet; that of the mouth of Cochetopa
Creek, 7,400 feet; and of the Grand Biver, at the mouth of the Eagle,
about 7,000 feet.
The division was constituted as follows, viz: Henry Gannett, topog-
rapher, in charge of party ; Dr. A. G. Peale, geologist ; Fred. Owens,
assistant topographer; Frank Kellogg, assistant; Arch. B. Balloch,
general assistant ; with two packers and a cook.
The part^' left Denver on July 21, travelt'd one hundred and fifty
miles to their field of work, commenced work August 3, ended work
October 29, and reached Denver about the middle of November.
On July 14, 1874, the San Juan ot third division of the United States
Geological and Geographical Survey left Denver for the field. Itconsisted
of A D. Wilson, topographer, directing; F. Bhoda, his assistant; F. M.
Eadlich, geologist; and Mr. Gallup, who was for a short time attached
aa barometric obsei'ver. The region assigned to this division was the
one generally known as the ^* San Juan countiy". In 1800 and 1861, a
10 GEOLOGICAL SURVEY OF THE TEBBITORIES.
party of prospectors, the "Baker's party'', bad reached a section of
country that was said to abound in silver and gold. After enduring
many hardships, a portion of the men succeeded in again reaching set-
tlements, while others were killed by the Indians. Ten years later, the
D)ining-region was brought into public notice a second time, more par-
ticularly hy the discovery and working of the " Little Giant" mine.
Since then, many prospectors and capitalists have examined the indi-
cations of ore, dud active mining has taken the place of mere prelimi-
nary examination. In 1873, the tract of land supposed to contain all
or nearly all of the metalliferous lodes was purchased from the Ute In-
dians by the United States Government. It was therefore one of the
main objects of the San Juan division to inquire into the geological and
mineraiogical characteristics of these lodes, with a view to obtain some
idea regarding their relations and value. A report thereon will be
found in the fourth chapter of the geological report of F. M. Endlich.
In every respect, the country surveyed was found to be of such extra-
ordinary interest, and the demand for information with regard thereto
was so apparent, that it was deemed advisable to publish at once a por-
tion of the results obtained. Bulletin No. 3, of the second series, 1875,
contains a drainage-map of the country ; a report by A. D. Wilson, re-
ferring to routes, roads, grades, etc. ; one by F. M. Endlich on the mines;
and an itinerary, together with hypsometric data, by F. Ehoda. All
will be incorporated in the subjoined report in their respective places.
While Colorado has furnished so many districts of rugged mountain
country, the one surveyed by this party during 1874 surpassed all. In
consequence of this character, it was not possible to complete so large
an area as was first intended, and about five thousand two hundred
square miles were surveyed. Of these, three thousand two hundred
were plotted during the winter following, and the geological report con-
fines itself to them. The remainder will be attached to the work of
1875, thus obviating the necessity of mapping an isolated area.
From the report and sketches accompanying, it will b^ seen that the
district was one of unusual character, containing i)henomena of great
geological importance. Enormous quantities of volcanic rocks were
found to form the highest peaks, reaching an altitude of 14,280 feet
above sea-level, while many unique features of detail were noted in the
same formation. Metamorphics and sedimentaries were also observed,
the former rising to very considerable altitudes. As might be expected
in a country so favorable to the formation of water-courses, the head-
waters of several large streams were discovered and mapped. Among
the most prominent are those of the Bio Grande, Eio Animas, Bio
Dolores, Bio San Miguel, Bio Piedra, and the Uncompahgre. Ethno-
logically, the southern section was found to present interesting data-
Through co-operation of the geological work with that of Mr. Wil-
son, the topographer, it became possible to render a geological map
that represents the horizontal distribution of the various formations
and their members, while sections display the vertical arrangement.
LETTER TO THE SECEETARY. 11
Ou October 19, 1874, the party again reached Denver, after having
completed the work above speciiied. During the season, sixty-five
topographical stations were made and seventy-four camps. Of these
stations, eighteen were over 13,000 feet above sea-level.
The photographic and naturalist's division was again under the
supervision of Mr. W. H. Jackson, the photographer, who has been
connected with the survey for the past five years in the same capacity.
The party organized in Denver, and took the field July 21. It com-
prised the photographer; Mr. Anthony, his assistant; Mr. E. Ingersoll,
naturalist ; and Mr. Frank Smart, assistant, with two packers and a
cook.
Middle Park was first visited, as it had not been worked up the pre-
vious season. A series of beautiful and very characteristic views of the
peculiar features of the park were secured, including views about Grand
Lake, the Hot Springs, the Great Gallon of the Grand, and the mag-
nificent mountain-forms and the charming vista as seen along the Blue
River. From the head of the Blue, the party progressed southward,
via the Arkansas, Poncha, and Gochetopa Passes, to the Los Piuos
agency Jbr the Ute Indians, where a series of views were secured
illustrating their life and peculiarities. The San Juan Mountains was
the next objective point. A camp was established in the upper end of
Baker's Park, in which was left all extra material in charge of two or
three of the men, and then, traveling with but few animals and very
light packs, rapid side-trips were made Juto all the strongholds and
fastnesses of the grandest mountains in all Colorado. Panoramic views
from the tops of the highest peaks were secured, illustrating, by bird's^
eye views, the geology and topography of the whole mountain-system.
Especial attention has been paid, all the time, to make these views
instructive as well as pleasing to the eye, and the system of panoramic
views which has been carrit^d out has been of very great assistance
to the topographers in working up their notes and expressing the
peculiarities of mountain-forms. To the geologist, also, they prove of
great value in recalling to the mud the surface-features, inclination of
strata, proportion of valley to mountain land and of timber to the rocky
summits lying above it.
From the permanent camp in Baker's Park, a side-trip was made into
the southwestern corner of the Territory, in search of the picturesque
aud interesting ruins of the habitations of a long-forgotten race. Ko
search was made until the Kio Mancos was reached; but, from this point,
ruins without number covered the plateau and filled the valle^vs aud
canons. Through the canons of the Eio Mancos, were found houses of
two stories in height, in the escarpment of the mesa, 800 to 1,000 feet
perpendicularly above the valley, of well-dressed sandstone, true in all
their angles, laid in a firm and ienacious mortar, and the inside
plastered and paneled in two colors. The greater msyority of these
houses were smaller, but as perfectly built as the larger ones, and all
12 GEOLOGICAL 8UBVEY OP THE TERRITOEIES.
were very difflcnlt of access, and resembled swallows' nests more than
anything else. To reach these with the photographic apparatus, it had
to be haaled up with long ropes taken from the pack-animals. From
near the mouth of the Rio Mancos, the party proceeded northwesterly
into Utah, finding group after group of towns and isolated watch-
towers perched upon great bowlders and upon the promontories of the
mesas. In one place was found a wall, evidently surrounding a town oi
a very considerable population, which was fully tweuty feet in thickness,
the outer surface of dressed stone, laid perfectly true, the space
between filled with large undressed blocks in adobe mortar.
The entire trip to these ruins, from and back to Baker's Park, com-
prised about three hundred and fifty miles of traveling. Only two
weeks could be devoted to it, which necessitated a somewhat- super-
ficial examination. Two series of views were made, the stereoscopic
and fiveby -eight plate. About forty negatives were made altogether,
illustrating perfectly all the leading features in a very unique series of
views.
From Baker's Park, the party returned by rapid marches, via the Rio
Grande, San Luis Valley, and Mosca Pass, to Colorado Springs, where
they met with the special party under my charge. Mr. Jackson joiued
him with his apparatus for a few days, while his party proceeded to
Denver and disbanded. The four or five days he was with the special
party, about one hundred additional negatives were made, mostly of
camp-life and the manner of conducting the various operations of the
survey while in the field. The result of the trip sums up as follows:
350 negatives, stereoscopic and five-by-eight, and the most extensive
and interesting conchological collection ever made in the Territories.
The party was out eighty-four days, making sixty camps, and traveling
one thousand two hundred and forty miles.
Not a negative was broken or lost on the trip, and the naturalist's
and different zoological and entomological collections came in safe.
The work of the survey during the season of 1875 will be extended
westward in Colorado to the meridian of longitude 109^ 3(K. The area
now remaining to be explored lies west of 108o on the western slope of
the main range of the Kocky Mountains and comprising the eastern por^
tion of the drainage of the great Colorado River. Hundreds of streams
of greater or less size cut deep gorges through this couptry in their
westward course to the Colorado River. There are some groups of
mountains yet to bo surveyed, but the highest peaks have already been
located.
According to the instructions given by the Department :
First. There shaH be tvo classes of maps : one known as " general *\ the other as
" special " maps ; and the " general " maps shaU be sabdivided into two classes, viz,
"topographical" and "geological".
Second. The ** general " maps shall be on a scale of fonr miles to an inch, or jb^aao*
The sheets thereof shaU be twenty-six (2<>) inches long by thirty-seven (37) inches
wide, including the border, and be folded once. The area to be represented on each
LETTER TO THE SECSETABY. 13
aheei shall be two and one-half degrees in longitude and one and one-fourth degrees
in latitude. The I12th meridian shall be taken as the standard from whioh the majM
aie to be projected in an easterly and westerly direeUon, aud the 38th parallel as the
standard from whioh they shall be projected in a uortherly and southerly direction ;
these lines forming the division-lines between the atlas-sheets adjacent thereunto.
Third. Maps or charts of the second or '* special " class may be constructed ou other
softies and embracing other areas, whenever it shall be found necessary for the purpose
of properly representing mining-districts, mineral, agricultural, pasture, or timber
lands, or for other q^ial purposes.
At the end of the next season, if suitable appropriations are made by
Congress for the purpose, the survey will have completed the most rug-
ged and mountainous portion of our continent, lying between meridians
1U40 3(y aiid 1090 30' and parallels 40o 45' and 40o 3(K. This will form
an atlas of six sheets, each comi)ri8ing about 11,500 square miles, or a
total of about 69,000 square miles. These maps are intended to express
not only the topographical features, but the geological also ; and, in
accordance with the directions of the Secretary of the Interior, these
charts will indicate the areas of grass, timber, and mineral lands, and
such other country as may be found to be susceptible of cultivation by
irrigation.
Numerous special maps of the mining-regions, isolated mountain-
ranges, and other localities remarkable for their complicated geological
structure, have been prepared on different scales. Much more of this
detailed study of interesting localities will be made when the final maps
are completed. Collections of great value were made in geology and
mineralogy, all of which will be reported on in due time.
Since the publication of the annual report for 1873, several volumes
have appeared in connection with the survey, which must be regarded
as of great value. Volume II of the quarto series, by Professor Cope,
on the "Cretaceous Vertebrata of the Western Territories", contains
304 pages text, with 57 plates. Volume VI of the quarto series, on the
** Cretaceous Flora of the Dakota Group", by Leo Lesquereux, constitutes
an original contribution to the vegetable paleontology of America, and
will prove very useful in fixing a most important geological horizon.
It contains 130 pages, with 30 plates. Much new material has come to
hand since the publication of that memoir, a portion of which will be
fbund in this report. A third edition of the " List of Elevations" and a
second edition of the " Catalogue of Photographs" have been printed to
supply the demand for the miscellaneous i>ublications. The most import-
antvolnmeof themiscellaneous series, however, isthe^Birdsof the North-
west", by Dr. BUiott Cones, which comprises over eight hundred closely-
printed octavo pages. Much of the text is written in popular style,
treating of the habits, or, as it were, the domestic life, of the birds ; and
on this account the demand for it among onr people has been unusually
gteat. Although it does not pretend to be a general work on the orni-
Ibology of the Western Territories, it contains a more or less complete
descriptive list of four-fifths of the birds of the United States.
14 GEOLOGICAL 8UEVEY OP THE TEBRITOBIES.
The memoirs that are either now in press or in an advanced state of
preparation are nnmeroas and important.
Volume IX, "The Fossil Invertebrata of the Western Territories," by
F. B. Meek, is nearly through the press. It will contain 45 plates, with
a great number of wood-cuts scattered through the te^t. Mr. Meek Las
most thoroughly elaborated every genus, and given the synouyuiy ot all
the species with unusual care. He regards this mem oirashis great life-
work, and it will add greatly to his fame as a paleontologist.
Volume X will be a " Monograph of the Geomitrid Moths'', by Dr. A. S.
Packard. It will form a memoir of ^50 pages quarto, with 13 plates,
on some of which are engraved one hundred figures. This work is now
rapidly passing through the press.
Volume VII, " The Fossil Flora of the Lignitic Tertiary Formation of
the Western Territories", by Leo Lesquereux, is intended to be a njono-
graph of that subject. It will contain sixty-five quarto plates, all of
which have been engraved by Messrs. Sinclair and Son, Philadelpbia.
Mr. Lesquereux is now at work on the text, and it is expected to be much
superior to the Cretaceous Flora, which was received with such marked
favor throughout the scientific world.
Volume VIII was originally designed to form an extended memoir
on the Fossil Flora of the Cretaceous and Tertiary formations of the
West, by Dr. J. S. Newberry. Twenty-six plates have been engraved,
and an edition of 2,500 copies printed for over ibur years. It is to be
hoped that some portion of this volume will be issued the 'present
season.
A very interesting memoir, in octavo form, entitled *'The Ethnog-
raphy and Philology of the Hidatsa Indians (Minnetarees of the XJp})er
Missouri) is now in the press. It was prepared at my request by 13r. •
Washington Mathews, U. S. A. Dr. Mathews spent some years at Fort
Berthold, on the Upper Missouri, as surgeon of the military post, and
his leisure time was devotQd to the study of the language and history of
this interesting tribe. An edition of lOO copies was printed by Mr.
Shea, of New York; but since that time Dr. Mathews has very much
enlarged and'improvod the memoir, and many portions af it he has en-
tirely rewritten. I had originally intended that it should be substituted
for a chapter I had written on this, many years ago, in a volume on the
Indian tribes of the Northwest, which is intended to form one of the
quarto series of the Survey ; but when I found the manuscript to be so
elaborate and complete, I preferred to issue it as a separate volume or
monograph. I am confident that this memoir will be received with
great favor, and that scholars in this country and in Eerope will be
profoundly grateful for this his labor of love.
The Bulletin of the Survey was originally started to embrace such
articles as demanded immediate publication on account of their i)ecu]iar
value or character. Many new species of animals and plants have been
collected from time to time, which needed to be published promptly to
LETTER TO THE SECRETARY. 15
secnre for the Survey that priority of discovery which is its right. The
first two numbers, issued during the year 1874, are not paged consecu-
tively; but those of the second series, which have been issued during
tbeyear 1875, will be paged consecutively, and the illustrations num-
bered, so that at the close of the year all the numbers may be gathered
together and bound in one volume. A title-page, table of contents, and
a complete index will be printed in the final number of each year. The
numbers for the year 1874 and 1875 may be bound together as volume I.
The irregularities in some of the publications are due to the unexpected
progress of the Survey and the acquisition of an unusual amount of
material.
The history of the Survey, from the small appropriation of $5,000 in
1807, was briefly told in the Annual Keport of last year. It has contin-
ued from year to year with a constant growth, though dependent upon
tbe annnal appropriation, Vhich will cease or be renewed each year at
the option of Congress.
Dnnug the years 1867 and 1868, the Survey was under the Commis-
sioner of the General Land-Office, and the two small annual reports
were incorporated in the annual volume of that Bureau.
In 1869, the Survey was placed under the Secretary of the Interior,
and the first independent annual report was made. When the demai)d
was so great that a reprint of the report of 1809 was ordered, I united
the two small reports of 1867 and 1868 with the report of 1869, as First,
Second, and Third Annual Eeports of the Survey.
Tbe original plan of the quarto seriea only extended to five volumes.
Volume V was to include all the natural history, and on tbe title-page
of volumes I and V it is stated that the entire series will be in five
volumes, of which the AcrididsB was to be the first part ; but the mate-
rials in all branches accumulated so rapidly that the number of vol-
umes was increased, and at the present time it will be limited only by
tbe duration of tbe Surrey.
The annual reports will be continued from year to year. Circum-
stances beyond tbe control of the geologist-in-charge may delay them,
as in the case of the present one, but they will appear as soon as they
can be prepared.
Besides the regular members of the Survey, there are several collabo-
rators, whose time is more or less occupied in the preparation of special
reports. Prof. Leo Lesquereux has been continuously connected with
the Survey for several years, with a regular salary, devoted to the elabo-
ration of reports on vegetable paleontology,' Mr. F. B. Meek has also
been a member of the Survey most of the time since 1867, with a fixed
salary, as paleontologist. Professor Cope has prepared the reports on
Vertebrata, and will continue to devote his time at intervals to that special
department. Dr. A. S. Packard spent several months during the past
aummer in Colorado, Wyoming, and Utah under the auspices of the
Survey, making large collections in his favorite branches, entomology
16 GEOLOQICAL SURVEY OF THE TEBBITOBIES.
and invertebrate natural history generally. The results of his labois
will appear in the annual reports, and in the beautiful quarto volume
on the Geometrid Moths. Mr. P. B. Uhler visited Colorado during the
summer. His collection of insects amounted to about 1,000 species.
In the Annual Beport for 1875, he will present- an elaborate essay on the
geographical distribution of insects. A very valuable paper on the
Hemiptera of our Western Territories appeared in No. 5 of the Bulletins
for the year 1875, illustrated with woodcuts.
Two volumes, quarto, by Professor Cope, are in course of preparation,
and will be published within a year if the Government provides the
money for completing the engraving : —
Volume III, " Vertebrate Paleontology of the Eocene Formations of
the West."
Part I. Distribution and Belations of the Tertiary Basins of the West
Part II. The Vertebrata of the Eocene.
Part III. The Belations of the Fauna of the Eocene.
Volume IV, *' Vertebrate Paleontology of the Miocene Formations of
the West."
Part I. The Fauna of the White Biver Epoch.
Part II. Tbe Fauna of the Loup Fork Epoch.
Part III. Tbe Belations of the Fauna of the White Biver and Loup
Fork Epochs.
The Survey is under great obligations to Dr. Elliott Goues, U. S. A.,
Mr. Bobert Bidgway, and Mr. Samuel H. Scudder, for very valuable
«
contributions to its publications.
The obligations of the Survey for favors of various kinds have been
numerous as usual, but few of them can be mentioned in this connection.
From D. Appleton & Go., of New York, very great assistance has been
received by permitting the use of the illustrations of Colorado scenery,
taken from their magnificent publication ^^Picturesque America.'' The
publishers of that work were permitted by the Interior Department to
use the photographs of the Survey on condition that the Survey should
have the electrotypes of the illustrations for use in the reports, and
some of the beautiful cuts in this report are the result of their gen-
erosity.
The illustrations for this report have been prepared in part, while the
text was passing through the press. This fact will account for irregu-
larities in the numbering of them. The pen-sketches and sections were
made by Mr. W. H. Holmes, a member of the Survey. For beauty and
accuracy they cannot be surpassed, and they add greatly to the value
of the report
To the Union Pacific, Denver Pacific, Kansiis Pacific, and Denver
and Bio Grande Bailroads, the Survey is under obligations for half-fare
tickets for its members.
The various changes which have occurred in the personnel of the
LETTER TO THE SECRETARY. 17
party duriDg the past year has thrown an immense amount of executive
labor on me, which has exhausted my strength, and consumed my
time to such an extent that 1 have not been able to give the necessary
att€^ntion and study to my portion of the report. The editing of so
many publications is sufficient labor for one person, and yet this is the
smallest duty that has devolved on the geologistin-charge. The various
executive duties, as correspondence, foreign exchange, settlement of
accounts, and the supervision of the parties in the field and office, seem
to increase from year to year, so that only mere fragments of my time
can be devoted to scientific study.
The present annual report is submitted with the belief that it contains
much that is new and interesting to geologists and the intelligent world
generally.
Very respectfully, your obedient servant,
F. V. HAYDEN,
United States Geologist
Hon. Z. Chakdler,
Secretary of the Interior.
2 H
4
Library. )
CIirPTER I.
/lUr.P HietTOKY OF THK LIGNITIC GKOUP ; FIRST STUDIKD ON THK UPPKR MrSSOCRI—
KAKI,Y VIKW8 ENTEKTAINKD BY ME£K, NKWBKKRY, AND OTHER PALEONTOLO-
GISTS ON THE AGE OF THIS GROUP— THE IJGNITIC GROUP OF THE NORTHWK&T
BEMKV£D TO BE CONTINUOUS SOUTHWARD WITH THE COLORADO AND LARAMI
BEDS. •
In this chapter, I desire to note, as briefly as possible, the progress of
the development of the Liguitic group of the Western Territories; aud
in doing so I need not go back farther in the past than the commence^
meut of my own explorations on the Upper Missouri in 1854. Prior to
that time, the observations that had been made by various travelei-s in
regard to the existence of coal-beds in different parts of the West were
of so indefinite a character that they cannot be used as evidence, though
they may form a part of the early history of discovery.
I have frequently stated in my former reports that I regarded this
group as, in many respects, the most im(K)rtant one in the West; that,
in its relations to the well defined Cretaceous group below it, it had a
more important bearing on the physical history of the growth of the
western portion of our continent than any other in the geological scnle.
Althoagh this formation has been studied with great zeal by several
parties within a few years, and most important additions to geology
liave resulted therefrom, there is evidently much more work to be done
before all the problems will be solved with sufficient clearness for onr
euiii-e satisfaction. That the evidence is very conflicting is shown by
the wide differences of opinion that are entertained in regard to its age
by geologists and paleontologists whose views have great weight in the
sejentific world.
The assistant geologists connected with the survey under my charge
bare been continually instructed to gather all the materials possible
beiiring on the age of this group, while Messrs. Meek, Lesquereux, and
Cope have been urged to study the subject from their own jieculiar
standpoints, regardless of unity of results. Many extremely valuable
anil instructive memoirs have already appeared in the reports of the
Survey touching upon this group, and several more are in process of
preparation or publication.
One fruitful source of difference of opinion has been in the nnsunder-
BtaDdingin regard to the different horizons of the coal-strata of the West.
That there are important coal-beds in rocks of well defined Cretaceous
age cannot be disputed, and I have long since yielded that point. What
we wish to show more clearly is that there exists in the West a distinct
aeries of strata which we have called the Liguitic group, and that it is
entirely separate, paleontologically and geologically, from a great group
of strata in the Lower Cretaceous, and perhaps extending down into the
Jurassic, which contains a great number of thick and valuable beds of
roah It is not necessary to discuss the question whether the term
Ligoitic shall be applied to the coa^ ot either or both groups. I have
used the term Ligniiic for the ujjper group without reference to the
19
20 GEOLOGICAL SURVEY OF THE TEKRITORIES.
quality of its fuel, simply to distinguish it from the other great group
of older date, the age of which is not questioned.
The time has now come, as it seems to me, when the materials are so
abundant that the subject can be reviewed with some care. It is well
known that I have held with some tenacity the ox)inion that the coal-
formations of the West are ot Tertiary age ; and I still regard the Lig-
nitic grou[) proper as transitional or Lower Eocene, and shall so regard
its age until the evidence to the contrary is much stronger than any
which has been presented up to the present time. When, however, the
proof is sufficient to decide the Cretaceous age of the group, I shall
accept the verdict without hesitation. It is somewhat doubtful whether
the age will ever be decided positively lo the satisfaction of all parties;
still we shall see in the course of this report that the character of the
paleontological as well as the strictly geological evidence is such that it
is not a matter of importance whether the entire group be placed iu the
Lower Tertiary or Upper Cretaceous, and it is most probable that the
testimony of the different paleontologists will always be as conflicting
as it is at present. • ^
In order that the reasons for my belief in the Tertiary age of the
Lignitic group may be more clearly understood and harmonized with
the present state of our knowledge of the subject, I will give a briei
history of the commencement and ])rogress of its examination.
My first knowledge of this group was obtained in the summer of 1854,
when I made a somewhat careful examination of the beds from tlieir
first appearance on the Missouri Eiver bear Fort Clarke to the mouth ot'
the Yi'llowstone, and thence up that river to a point near the mouth of the
Big Horn. In all this distance, about six hundred miles, following the
windings of the river, the Cretaceous beds appear but once, and then only
along the bed of the river for a few miles, while the entire country, with
thisexception, is occupied with the Lignitic group. . The area of thisforma-
tion on the Upper Missouri cannot be less than one hundred thousand
s()uare miles, and extends far north across the northern boundary of the
U uited States into the British possessions. This group everywhere rests
upon well-defined Cretaceous beds, which we haveail along regarded as the
highest kuowMi in the West, and have received the name of the Fox
Bills group, from a locality on the Missouri Biver called the Fox Hills,
or Fox Kidge, where this formation was first studied, and was very lull
of molluscan life. There is a gradual passage upward Irom the black
plastic, shaly clays of No. 4, or the Fort Pierre group, to the yellow cal-
careous clays of the Fox Hills group, and at the upper portion, t'he
sediments are arranged in thin layers, very 'arenaceous, and indicative
ot their deposition in turbulent as well as shallow waters. In these are-
naceous sediments, the well-marked marine, life ceases to exist, and soou
alter appear the brackish-water species. Between the Big Cheyenne
and the Moreau Rivers, branches of the Missouri that come in from the
west side, the Lignitic strata overlap those ot Cretaceous age, and in the
lower beds occurs a species of Ostrea associated with some other brackish-
water forms. I am not positive as to the exact position of these fossils,
but I am confident that a bed of gray sandstone, with a layer of imjiure
coal or Lignite lie, below any of the brackish- water forms found in the
Northwest. Scattered over the weathered surface of these Lower Lig-
nitic beds, and believed, without doubt, to have been originally
imbedded in them, were found several specimens of Vertebrata which
have been regarded by Professor Cope as characteristic of the Creta-
ceous era. So far as the Northwest is concerned, the brackish-water
beds are not more than 200 feet in thickness, while those that are
HATOEs.] GEOLOGY AGE OF THE LIGNITIC GROUP. 21
pnrely fresb-water raust reach an aggregate thickness of 3,000 to 5,000
feet. During the years 1854 and 1855, 1 stndied this group on the Mis-
souri to Fort Benton, and on the Yellowstone, where it is most exten-
sively developed, to the month of the Big Horn River and collected great
qoautitie8 of animal and vegetable remains from the base to the summit.
Every season, up to the antnmn of 18G0, I made collections from this
group in all parts of the Northwest.
The vertebrate remains were studied by Dr. Leidy ; the vegetable
fossils, by Dr. Newberry and Mr. Lesquereux^and theinvertebratelossils,
by Mr. Meek and the writer. None of us even doubted their Tertiary
age. Numerous papers were published by Mr. Meek and the writer
on the geology and invertebrate paleontology gf this region in various
journals, but mostly in the Proceedings of the Academy of Natural Sci-
ences at Philadelphia; and inasmuch as these articles arer not easily
accessible to the general public, 1 shall be excused from quoting par-
agraphs from them quite ireely in an official report.
In an article published in the Proceedings of the Academy of Natural
Sciences, May, 1857, we siate that of the 150 species of Mollusca already
described, 54 species are of Tertiary age, 50 are strictly freshwater, anil
only four belong to genera supposed to inhabit salt or brackish waters.
This group was even regarded as of Miocene age. The first conclusion,
at the close of this i)aper, reads as follows : — " We have no evidence that
any of the Tertiary deposits now known in Nebraska are older than
Miocene."
The above paragraph shows that Mr. Meek and the writer attempted
to correllato the various Tertiary groups in the Northwest in the light of
the knowledge they i)ossessed at ihat time.
Bat it was from the very abundant fossil flora of this group that the
most positive proof of its age was derived. It is hardly possible to
estimate with accuracy the thickness of this great group in the North-
west, but I should regard it from 3,000 to 5,000 feet in the aggregate,
with from twenty to thirty beds or seams of lignite, not including the
thin seams of an inch or two, which are very numerous. These vary
from six inches to ten feet in thickness.' All through this great thicks
ness of strata, the leaves are found in most instances in a remarkably
j)erfect state of preservation. • Sometimes they are so abundant and
80 perfectly preserved th''t they would appear to have fallen from
the trees on the spot and in the greatest profusion. It is not uncommon
for a stratum of two feet or more to be composed almost entirely at*
these leaves, lying parallel with the layers, as if they had not been dis-
turbed after dropping froni the trees. Along the immediate vicinity of
the main rivers (Missouri and Yellowstone), these plants are the most
abundant, far more so than in the more important coal-regions of
Wyoming or Colorado.
Although my own collections, made from 1850 to the autumn of 1860,
doubtless comprise the greater part of the species that will herealteV /
be found, and therefore form a permanent basis for determination and
comparison, yet the force of their teachings is somewhat weakened from
the fact that the species from difi'erent horizons were not kept suffi-
ciently separate. We know, however, that some of the species have a
very great vertical as well as horizontal range, and that, so far as can
be detected, there is no break in the sequence of the beds from the
Siiskatcfaewan to Santa F6.
The following extract is taken from a paper prepared by Mr. Meek
and the writer, and published in the proceedings of the Academy of
Natural Sciences, Philadelphia, December, 1861. This extract will not
22 GEOLOGICAL SURVEY OF THE TERRITORIES.
only serve to sbow the views we entertained at that time after .*
study and discussion of the invertebfite fossils, but incident
opinions of other eminent paleontologists:
"It would extend these remarks beyond the limits assigned t
attempt any detailed account of thi* Tertiary rocks of Nebraska
discuss at length the question respecting their relations to those
Atlantic coast, or of the Old World.
" We must, therefore, limit ourselves here to a few brief statemc
leading facts, and leave all details for another occasion.
" In the first jdace, we would remark, that no strictly marine Te;
deposits have yet been discovered in all the Rocky Mountain regi
•Nebraska, nor, so far as known, in any other portion of Nebr*
Kansas, or Utah.
" Throughout all this great central area of the continent, wherevei
oldest Tertiary deposits have been seen, they give evidence of fresh,
brackish water origin, and, where observed resting upon the most reci
Cretaceous beds, the two have been found conformable, and sometim
blended together, so as to render it difficult to draw a line betw^eeu the.
in the absence of organic remains. All the facts indicate a gradual
change from the marine conditions of the Cretaceous ; at first to brack-
ish, and then to the fresh-water conditions of the Tertiary. The pre-
dominance of Gasteropoda and Lamellihranehiaia^ and the comparative
paucity of types usually considered characteristic of deeper water
deposits, as well as the coarser nature of the sediments, near the end of
the Cretaceous epoch of this region, indicate that the waters were grow-
ing more shallow as the land on the east encroached on the sea, and
islands were rising where the Bocky Mountains now stand, while the
close of the Cretaceous period seems to have been attended 'by the grad-
ual elevation of large areas of country here above the ocean-level.
This and other contemporaneous changes of physical conditions caused
the total destruction of the whole Cretaceous fauna.
"After this, extensive tracts of country in the region of the Rocky
Mountains, and east of them in Nebraska and other northwestern Ter-
ritories, w ere occupied by bays, inlets, estuaries, etc., of brackish water,
inhabited by MoUusca of the genera Ostrea, Unio^ Fisidium, CorhicuUij
Potamoniyaj Melania, Melamptis, VimpuYay etc., all of Tertiary types.
As the gradual elevation of the conntry continued, the salt and brack-
ish waters receded and gave place to lakes and other bodies of fresh-
water, in which most of the Tertiary rocks of the Northwest were
deposited ; so that in all, excepting the earliest Tertiary beds of this
region, we find only the remains of strictly fresh-wat^r and terrestrial
animals.
"The passage from the brackish to the fresh water beds in the oldest
member of the Tertiary of this region seems not to be marked by any
material alteration in the nature of the sediments. Nor have we, so
far as is yet known, any reasons for believing that any climatic or other
important physical changes, beyond the slow rising of the land and the
consequent recession of the salt and brackish water, took place during
the deposition of the whole of the oldest member of the Tertiary here,
since we find a considerable portion of the species of fresh-water Mol-
lusca ranging through this whole lower member.
"The principal difference between the fossils of its upper and lower
beds consists of the gradual disappearance of strictly brackish-water
types as we ascend from the interior strata. The entire series of Ne-
* The old Territory of Nebraska is here referred to.
BATUIC5.]
GEOLOGY — LIGNITIC GROUP.
23
braska Tertiary rocks cousistsof three or four groups, three of which
at least (and probably four) evidently belong to separate and distinct
epochs. They usually occur in isolated basins, but have, with one ex-
ception, all been seen in such connection as to leave no doubt in regard
to their order of superposition.
'^ Their prevailing lithological characters, estimated maximum thick-
nesses, and order of succession will be seen in' the section given below.
a
c
?5
Sabdivisionf.
C
LocAlities.
5^
Fine looM naod, with some lAyors of limentone ;
contains bones of Canity Fe\is, (kutor, Eqmm,
Ma»todon, Teghido, etc., some of which are
acarotily distingaishable from living secies.
>
White and light drab clays, with some beds of
sandstone tud local layers of limestone ; fos-
sils, Oreodon. TUanotheriwn, Ohceropotamua^
Shinoetroa^ AnehUherium, Hyaenonodon, Ma-
ehttirodut, Trionyx, Tegtiido, Bdix, Planorbie,
Limnfea, petrifleu wood, etc., etc. All extinct.
No brackisb-water or marine remains.
d
IS.
4
OS-
b s
s c
light gray and ash -colored sandstones, with
more or less argillaceous layers. Fossils,
fragments of Tritmyx, Testudo, with large He-
lix, Vivipara, petritied wood, etc No marine
or brackish-water types.
Beds of clay and sand, with roand ferruginous
concretions, dnd nnmorons beds, seams, and
local deposits of lignite ; groat nnmliers of
dicotylcuooous loavcN, stems, etc., of tho gen-
era Platanua, Acer, Ulmuf, Popuhu. etc, with
very large loaves of tme fun palms A\9o,
Helix. Mdania, Vivipara, CorbictUa, Unio, Oh-
treOy Pofamotnt^a, and scales of If^puiohtf, with
bones of Trionyx, Emy»^ Comptemye^ trocodi-
hu, etc.
I
o
o
a
8
at
On Lonp Fork of Slatte River,
c<x:ending north to Niobrara
River, and south to an un-
known distance beyond the
Platte
Bad Lands of Whito River, un-
der the Loup River beds on
Niobrara, and across the
country to the Platte
Wind River Valley, also west
of Wind River Mountains.
bio
-"I
a
Q
u
o
s
u
o
■♦a
S
o
©f
Occupies the whole country
around Fort Union, ext<'n<1-
ing North into tho British
poHaessions to unknown din-
tances: also southward to
Fort Clarko ; seen under the
Wiiite River group, on North
■ Platte River, abovi* Fort Lar-
amie ; also on wr st side of
Wind River Monntalns.
o
a
9
'•The Fort Union, or Great Lignite group, occupies extensive areas of
coantry in Nebraska, and has been seen beneath the White River group
at several distant localities. It was evidently deposited in large bodies
of wat«r, which were at first brackish, and then gradually became fresh.
''The great number of fossil leaves, and numerous beds of lignite con-
tained in it, clearly show that the shores of these ancient estuaries,
lakes, etc., in which this formation was deposited, supported dense
forests of large trees, and a growth of other vegetation, far exceeding
in luxuriance anything now met with in these latitudes.
"Indeed, the presence of true fan palms, of large size, and the remains
of the genus Crocodilus^ as well as the affinities of the Mollusca found
in these beds to southern forms, all point rather to the existence here of
a tropical than a temperate climate during their deposition. In regard
to the relations of this formation to known horizons in the Tertiary of
the Old World, we scarcely feel prepared to express a very decided
opinion.
"The difficulty in the way of drawing inferences bearing on this point
from the remains of Mollusca found in these beds is that they, being
fresh and brackish water types, bear little or no analogy to those of the
24 GEOLOGICAL SURVEY OF THE TERRITORIES.
Tertiary of the States bordering on the Atlantic, nor are any of them, so
far as known, specitically identical with foreign forms.
''When we bear in mind, however, the fact, that wherever this forma-
tion has been seen in contact with the latest Cretaceous beds, the two
have been found to be conformable, however great the upheavals and
distortions may be, while at the junction there seems to be a complete
mingling of sediments, one is strongly impressed with the probability
that no important member of either system is wanting between them.
This view is also rendered more probable by the fact that the formation
under consideration is known to hold a position beneath the White River
group, which is characterized by the remains of an entirely different
launa, clearly of Miocene age.
** Again, the occurrence in ihis lower group of remains of the genus
LepidotuSj which is, we believe, in Europe unknown above the Eocene,
while the other vertebrate remains found associated with it have been
compared by the distinguished comparative anatomist, Professor Leidy,
with types even older than the Tertiary, are facts strengthening
the impression that this Fort Union Lignite group probably repre-
sents the Eocene of Europe.
" It should not be forgotten, however, that an extensive and beautiful
series of fossil plants from this formation, although not yet thoroughly
. investigated, have been thought by Dr. Newberry to be most analogous
to Miocene types.
"Yet even if this formation should prove to be of Eocene age, this
would only be in accordance with what is now known in regard to the
earlier introduction of particular types of plants in the Cretaceous sys-
tem of this country than in that of the Old World.
" As the Wind River deposits have not yet been seen in contact with
any well-marked beds of the other Tertiary formations of this region,
and few fossils have yet been found in them, their position in the
series remains doubtful. It is, therefore, only provisionally that we
have placed this formation between the Fort Union and White River
groups in the foregoing section. It may possibly belong to the horizons
of one of these rocks, or even rei)rese!it them both in part, or, what is
more probable, it may occupy an intermediate chronological position.
" The only fossils yet found in this formation are fragments of Trionyx
and Testtido^ together with the shells of two species of Helix and a cdst
of H Vivipara, One of these Helices is more like H\ Leidyi from the
White River group than any of the other species yet known from any
of these rocks, while the other is a very large depressed species of
southern type, quite unlike any of those hitherto found in any of the
other Nebraska rocks. The Vivipara seems to be indistinguishable
from our F. trochiformis from the Fort Benton group, though, as it is
a mere cast, it cannot be identified with certainty with that
shell. No marine or brackish-water fossils have been found in these
beds. The White River group is the formation that has furnished the
extensive and interesting collections of vertebrate remains which have
been so ably investigated by Professor Leidy. It occupies a consider-
able area in the region of White River, and is seen beneath the succeed-
ing formation on the Niobrara and Platte Rivers^ Irs position above
the Fort Union or Great Lignite group has also been clearly and satis-
factorily determined.
*' This formation is mainly composed of a series of whitish, indurated
clays, which have been worn and cut. by the streams, rains, and other
atmospheric agencies, into numerous deep valleys and ravines, so as to
leave various peaks, isolated columns, towers, etc., presenting, as seen
HATDCf.) GEOLOGY ^WHITE RIVEE GROUP. 25
from a dfstauce, exactly the api)earance of tbe ruins of ao ancient city.
Thcfdifficalty the traveler meets with in finding his way through this
interminable labyrinth caused the Indians to call it, in their own
laugoage, th^ Bad Grounds ; hence the French name, Mauraises terres^
applied by the Canadian voyageurs in the employ of the fur-companies.
^^ Tbe vertebrate remains found iu these beds belong to the gcDera
OreodoUj AgriocharuSj Pabrotherium^ LeptomeryXj Leptanchenia^ Pro-
tomeryxy Merycodos^ Titanotheriumj Leptochcerus^ Hyracodon^ Enttlo-
doH^ PalcBOchcertu^ Rhinoceros^ Steneojiber^ Machairodos^ Anchitheriunij
Hyopotamus^ Hycenodon^ IschyromySj Palceolagwt^ Eumys, Teatudo^ etc.,
Hc. The alfinities of these fossils, as has been shown by Professor
Leidy, clearly establish the Miocene age of this formation.
** Comparatively few invertebrate remains have yet been found in the
White River group. They consist of one species of Uelix^ one or two of
Limncea^ a small PhysOj two or three small species of PlanorbiSj etc. No
iaml leaves nor t)eds of lignite have been met with ii> it, and all the
animal remains, as may be seen from the foregoing list, are terrestrial
and fresh-water types. The Loup River beds consist mainly of incoher-
ent materials, and were evidently deposited after the upper surface or the
White River group had been worn into ravines and other depressi(ms.
It occupies much of the surface of the country in the region of the Loup
Fork and Platte River, and exten<ls far south of the latter stream.
"The vertebrate remains from it described by Professor Leidy belong
to the genera MegalomeryXy Procamelus^ CermtSj Rhinoceros^ Mastodon,
Ekphas^ Hipparion^ Merychippus^ Equus^ Castor^ Felis^ Canis^ Testudo^
etc., many ol which are very closely allied to recent species. A few shells
of the genera Helix^ Physa^ etc., apparently identical with living spe-
I'ies, have also been found in these betls. All the species of vertel)rate
and other remains yet found in them are distinot; from those occurring
in I he White River group and beds below, and they have not yet afforded
any brackish or marine ty pes of any kind.
^^ When we take into consideration the position of this formation above
the well-marked Miocene White River group, and the relation of its
orpianic remains to Pliocene and recent species, there is little room for
doobting the correctness of its reference to the horizon of the Pliocene
of Europe.
''The extracts which I have given are suflScient to show the opinions of
a most excellent paleontologist in regard to the age of this group as
interpreted from the invertebrate fossils.'*
Let us for a moment glance at the testimony of American vegetable
paleontologists. Without quoting again, I will simply refer the reader
to the interesting report of Dr. J. S. Newberry on the Cretaceous and
Tertiary plants collected by me during the expedition to the Yellowstone
and Missouii Rivers, during the years 1859 and 1^60, a portion of which
was reprinted in the Annual lieport of W^yoming, 1870, coinmeuciug at
Piige 94. It will be seen that Dr. Newberry regarde<l these fossil plants
a^iiot only of Tertiary age, but Middle Tertiary, or Miocene. In itn in-
teresting 'memoir published iu the Annals of the Lyceum of Natural
History, in 18G7, Dr. Newberry remarks :
"By' far the largest representation of our Tertiary flora is, however,
ooQtained in collections made by Dr. Hayden on tbe Upper Missouri, of
vhich the greater number of species are described iu the present mem-
oir. These plants are from the lignites proved by the associated fossils
to be of the Miocene age. They were collected at various points on the
Missouri River, at Fort Clarke, at Red Spring, thirteen miles above, at
Fort Berthold, at Grow Hills, one hundred miles below Fort Union, at
26 GEOLOGICAL SURVEY OF THE TERRITORIES.
the mouth of the Yellowstone, on O'Fallon's Creek, one hundred miles
above the mouth of the Yellowstone, and in the valley of that stream.
^^ The explorations of Dr. Hay den prove that this Miocene Lignite for-
mation occupies the beds of extensive lakes, which formed «basins on the
surface of the continent when it had but recently emerged from the
Cretaceous sea. As has been remarked elsewhere, the lower members
of the series contain a few estuary shells, showing the access of salt-
water at that period ; but during the deposition of by far the greater
portion of these beds, the water of the ocean was entirely excluded from
the basins in which they accumulated. There is, therefore, every reason
to believe that the debris of ligneous plants which compose this collec-
tion were derived from trees which grew along the shores of the lakes
and streams of the Tertiaty continent; that then, as now, alternations
of seasons prevailed, by which the foliage of these trees were detached
by an autumnal frost, and that falling into the water beneath or near
them, and sinking to the bottom, they were enveloped in mud, precisely
as leaves of our sycamores, willows, oaks, etc., accumulate at the bottoms
of our streams and lakes of the present day."
I need not extend these remarks farther to illustrate the views of
both paleontologists in regard to the age of the Lignitic group, as
observed in the Northwest, up to within a comparatively recent period.
1 need not refer to the views of Mr. Lesqnereux, inasmuch as they have
been consistent in the belief of their Tertiary age, from the commence-
ment of his examination up to the present time, and his arguments in
favor of this belief have been set forth in nearly all the annual reports
of the Survey.
If the Lignitic group, as developed on the Upper Missouri, is admit-
ted to be either entirely or in part of Tertiary age, the question will arise,
what bearing has this .admission on the age of the coal-beds of Wyo-
ming .and Colorado!
I beg just here to call the attention of geologists to the geological
maps prepared by me, and published in the Final Report of Nebraska,
1869, and in the Geological Ueport of the Exploration of the Yellowstone
and Missouri Rivers, 1859-'60, especially the latter map. It will be seen
by the last-named map that the Lignitic group occupies a very large area
along the Upper Missouri and the Yellowstone Rivers, that it ext^euds
far north into th^ British possessions. We may then trace it south-
ward in a broad continuous belt across the Yellowstone River, between
the Black Hill^and the Big Horn Mountains, until it is overlapped b^
the White River group, about sixty miles north of Fort Laramie. If
we continue southward along the east base of the Laramie range, we
find that the Lignitic group reappears about ten miles south of the
Union Pacitic Railroad. We find that where the White River group
and the Lignitic groiy) come in contact, the former is superimposed on
the latter, and that really the White River group formed a vast basin
subsequent to the existence of the great lake in which the lignitic
sediments were deposited. We find also, by examining the White River
group along the base of the mountains, that the Laramie range formed
a barrier that prevented it from extending into the Laramie Plains ;
but the evidence is clear that, at the time of the existence of the
great Lignitic lake or sea, this barrier did not prevent the water-
communication with the Laramie Plains. Indeed, the evidence seems
quite clear that, with the exception perhaps of some isolated peaks ris-
ing above the waters, there was no mountain-barrier where we now
have the Laramie range. Theretbre, with the exception of the Bear
River and Coalville group, we may conned the coal-bearing beds of the
HATDCX.]
GEOLOGY COAL ST'RATA.
27
Laramie Plains and Colorndo with tbe vast group in the Northwest. I
Lave traced this geographical connection stei> by step over this great
area, have studied the formation with some care, and collected both
vegetable and animal fossils in the greatest abundance from point to
point. I would say, however, that comparatively few of the fresh-water
$per*ie8 of Mollusca, so abundant in the Northwest, are found either in
Colorado or the Laramie Plains; but it possesses the same character,
and many of the same species of plants are scattered all over this im-
mense area.
CHAPTER 11.
THE LIGNITIC GROUP AS EXAMINED AT CANON CITY — COTjORADO SPRINGS— NORTHWARD
TO CACHE LA FOUDUE CREEK — MONUMENT CREEK GROUP^ PROBABLE AGE OF
THESE GROUPS.
Our examinatioDS along tbe eastern base of tbe mountains in Colorado
were directed mainly to the tracing-out of the connection between the
Liguitic group and the older beds. We traced the boundary of this
group, with great care, from Canon City, on the Arkansas River, north-
ward nearly to Cheyenne. It is hardly ix>ssible that any links in the
chain of evidence escaped us, and the principal dill'erences of opinion
now will consist in the degree of importance to be attached to that evi-
dence. The question is whether tbe coal-bearing strata known as the
Lignitic gioup of the Eastern Rocky Mountain region is of Cretaceous
or Tertiary age. In this chapter, we shall simply record our field-obser-
vations, referring the reader to a subsequent chapter lor a brief discus-
sion of the question of age.
South of Canon City, on the south side of the Arkansas River, there is
an isolated coal-basin occupying an area of about fifty square miles. Tlie
strata lie for the most part in a nearly horizontal position, indicating no
great disturbance, except along the north and west sides. On the north-
west side of the basin, along the i mmediate base of the mountains, the beds
have been lifted up, so that a great thickness of the Lignitic sandstones is
exposed, at least 1,000 to 1,500 feet. The Cretaceous beds are also seen
lying close to the flanks of the mountains. As we proceed southward
along tbe junction of sedimentary beds and the granites, the Cretaceous
beds disappear, and one by one the lower Lignitic, until the whole
mass juts against the granitic rocks, with no perceptible evidence
of disturbance, except in a general way. There seems to be a rapid
Klope froni the base of the mountains to the Arkansas River, a dis-
tance of about five miles, thus giving to the strata a general dip of
about 50. So far as we could ascertain, tbere are no coalbeds'ia
tbe noitbern portion ot the basin. Tbe rocks consist mostly of rath-
er tbick beds of gray, brown, and yellow sandstone, with loose clays
and sands between, but no coal beds. We find that the coal-bear-
ing [)ortion does not occupy the entire area, and that a large part is
classed as barren coal-measures. The most important coal-mine has
been opened on the east side of the basin, about midway, on Oak Creek.
This is one of tbe most important coal-mines in the Territory. It was
described briefly, but quite clearly, in the Annual Report of tbe Survey
for 1809, and since that time in the more elaborate reports of Mr. Les-
quereux. In tbe summer of 1872, Mr. Lesquereux made a careful
examination of tbe coal-formations all along the east Imse of the Rocky
Mountains from Cheyenne to Santa F6. His report in tbe Annual Re-
port for 1872 is quite exhaustive. Tbe section of the coal-strata on
page 323, made by Mr. J^eilson Clark, the superintendent of the mines, is
more accurate than any other that has been made of tbe group, and need
not be repeated here. It remains now to consider tbe beds below this sec-
28
BAWK-l GEOLOGY LIGNITIC GROUP IN COLORADO. 29
ion, which are supposed to be of Cretnceoaa age, but which might very
properly be called beds of passage from well-marked Cretaceous j^trata to
those containiug coal and vegetable remains. We have heretx)lore <le-
scribed the Upper Cretaceous beds as of strictly marine origin; that tlie
sediments were deposited in a broad and, at least, moderately deej) sea.
As long as we find that these physical conditions prevailed, we observe a
gi eater or less abundance of fossils of strictly marine forms, as Ammon-
iies^ Baculites^ Inoceramus^ etc,; but even when no break can be found m
the sequence of the beds, indicating a lapse of time in the deposition of
the sediments, we discover that the physical conditions gradually change
outil there is a complete extinction of all marine forms of life. We find
here on the Arkansas River a full development of the Upper Cretaceous
formations Nos. 4 and 5, with their peculiar fossils. W^e also observe that
the materials of the upper portion of No. 5 pass gi adually from a dark-
yellow clay to a rusty-yellow sand, and above this, 200 to 300 feet, of a
aort of irregular thin layers of mud like material, with curious concre-
tions of sandstone. In this group of strata, which may be called transi-
tional, not a fossil has yet been found to prove the age beyond a doubt.
Easting on this irregular group of mud-strata is a bed of sandstone of
very vaiiable thickness as well as structure. Sometimes it is^ot more
than dO feet thick, and then again it is 300 to 400 feet thick. It is full
of rounded concretionary masses, and shows very clearly that its sedi-
ments were deposited in shallow and very turbulent waters. This sand-
stone passes up into clay, and on this clay rests a bed of coal. In the
bed of sandstone below the coal, the peculiar vegetation of the Lignitic
group is found in considerable abundance, and, therefore, this may mark
the lowest horizon ot this group. Now, whenever, in any part of the
country, invertebrate remains of any kind are found above this bed of
sandstone, they are invariably brackish or fresh water in their charac-
ter; and whenever any of these fossil shells are observed below this sand-
stone, they are always strictly marine. We have in the vicinity of these
coal-mines the details of structure, which we have briefly described
above, most clearlj' shown. Now the question arises, what stress shall
be laid on these remarkable physical changes ? W^ould not this form an
excellent line of separation between two great periods in geological
timef Are not these changes sufBcient to indicate clearly that these
are probably the beds of passage or transition between the Cretaceous
and the Tertiary epochs ¥ We find also a complete change in the vege-
table as well as animal life. We are not aware that any of the verte-
brate remains, which have been regarded by Cope and Marsh as proving
the Lignitic group to be of Cretaceous age, Lave ever been- found mingled
with any other forms of life of strictly marine origin. So far, all the
vertebrate fossils have been discovered in the Lignitic group. It seems
therefore that not a single species of vegetable or animal life survived
the physical changes which were introduced during the time of the depo-
sition of the transition group. Now, if we have shown this state of
affairs in regard to the Caiion group, we may connect this group easily
with the Raton Hills group to the southward, and the Monument Creek
groap far to the northward near Colorado Springs.
In passing northward, we see no more of the Lignitic group, so far as
we have examined, until we reach Colorado Springs, a distance of thirty
uules in a straight line. Here it is exposed in the form of an irregular
bluff ridge, running down from the base of the mountains a little south-
east, beyond the limit of our explorations up to this time. In section 2,
we see in the foreground, at either end, the form of the sandstone blufls,
which appear to be remnants of a far more extended group of strata.
30 . GEOLOGICAL SURVEY OF THE TERRITORIES.
The inclination is slight, 5° to 10^, about ; northeast. The bluflf-wall
undoubtedly extended at one time over the entire interval south and
southwest and was joined to the Caiion City group ; the intervening por-
tions having been removed by erosion, with the exception of a narrow
belt just at the base of the mountains. This interval is entirely occu-
pied with Cretaceous rocks at the present time. The valley of the
Fountain, as well as that of Monument Creek, for some distance above
its junction with the Fountain, is underlaid with Upper Cretaceous
groups Nos. 4 and 5 ; but the surface is everywhere so denuded and
grassed over that the junction of the Cretaceous with the Liguitic group
is nowhere wdl marked.
- The lower bed of sandstone, which is usually regarded as the com-
mencement of the Lignitic, iscomposed sometimes of yielding arenaceous
sediments, and therefore cannot always be relied upon as forming a fixed
horizon of demarkation. But, in the majority of instances, this floor of
sandstone is present with a greater or less thickness. About ten miles
east of Colorado Springs, some very important coal-beds have been
opened by Mr. Matt France and others. This locality is a very import-
autone for the studyof this great coal-group. Between Colorado Springs
and the eoal-mines, the intervening country is very rolling or undulating,
and so grassed over that no sections of the underlying beds are exposed ;
but, before reaching the mines, the rounded grassy hills are covered with
fragments of calcareous concretions, from which have been taken a great
variety of the fossils characteristic of the Upper Cretaceous. The three
forms which are usually so abundant, Ammonites Lohatus^ Baculites ova-
tu9^ and InoceramMS, are here found in great numbers. This point is about
600 feet higher than Colorado Springs ; and inasmuch as the strata are
horizontal, we may estimate the thickness of the Cretaceous beds above
tlie vallev of Monument Creek at GOO to 800 feet. As we continue to
the west we soon come to dark, rusty-brown sandstones, with great
numbers of a peculfar kind of sea-weed, called by Mr. Lesquereux Ilaly-
menit€8. There is a series of alternate layers of airenaceous clay and
sandstones, 200 feet or more in thickness, the upper portion containing
vast globular concretions, as illustrated in Plate 4, Fig. 2, which corre-
spond to the mud-beds seen in the vicinity of the coal-basin of the
Arkansas. A section of the beds here would be as follows, in ascending
order : —
Section a.
Ft. In.
1. Coal S .0
.2. Clay •.. 6 0
3. SaDdstoue 7 0
4. Clay 10 2
5. Yellow saDdBlone i 5 0
6. Solid coal 8 1
7. Rusty- browD cla.v and sandstone 50 — 80 0
8. Altercate layers of sandstone and clay 200 0
9. Cretaceous tomiations Nos. 4 and 5 GOO— 800 0
This section is in part constructed from shafts that have been sunk
for coal. So far as I have observed, the only way to obtain a clear sec-
tion of the coal-strata, is by boring or sinking a shaft. All other sec-
tions, unless made in some actual cut, may be regarded as only ap-
))roximately correct. The lower portion of section a. Cretaceous, grad-
ually passes up into bed 8, which is composed at the bottom of alter-
nate thin layers of sandstone and clay, these layers increasing in
tlii kness toward the top. The upper portion is made up mostly
of rounded concretions, varying in size from an inch or two to sev-
ShoKiing the variability of the Ziignitic beds.
Parallel sections taken on the face of Pulpit Bock
5 mile* north of Colorado Springs through identical
strata and only ^feet apart.
/
I * . -• u ;, r
^•\
.« *
/
v.. ■'• ■
HATDKsl GEOLOGY — ^LIONITIC GROUP — ^SECTION. 31
ehil feet in diameter. Sometimes these concretions are oval or flat,
with horizontal layers; bnt in most cases they fall in pieces, showing
ooocentric coats, the disk like shells falling off from the outside gradu-
ally. There is also a species of sea- weed, HalymeniteSj quite abundant
in these sandstones. I call them the transition beds, though they may
be Cretaceous, and they correspond with those described as occurring
below the coal on the Arkansas.
Number 7 in the section is the sandstone that usually forms the basis
bed of the Lignitic group. This bed is here full of small iron-rust con-
cretions, some of them solid, with a gray nucleus, others hollow, the
cavity Ailed with fine dust, a kind of iron-rust. These concretions, vary-
m^ from an inch to three or four inches in diameter, are so abundant that
they cover the ground for some distance from the bluff. About the mid-
dle of the sandstone-bed, there is a band of dark-brown indurated sand,
mixed with bits or fragments of vegetable material, about five feet in
thickness. This bed or band may, quite possibly, become coal in some
localities. At one point in the southern i)ortion of the coal-basin on
the Arkansas Biver, a seam which appears to correspond to this dark
band occurs in the lower sandstone, and is quite good coal, two feet in
thickness. The quantity and character of the coal at this locality was
determined by the sinking of several shafts. In section a, we have
ttro quite thick beds of coal, both of which were penetrated by a shaft,
and thus the section may be regarded as correct.
»
Section &.
Feet
1. Sarface-8oi1 8
2. Sand 12
a Drab-clay 6
4. Soapstone and clay 9
5. Slate 5
6. Sandstono 4
7. Arenaceous clay 7
8. Soft slate C
9. Coal 1
10. Sandstone with plants ; 30
11. Bitominous shales 11
12. Sandstone with iron 3
13. Clay G
14. Hard black slate 11
13. Coal 6.
In section &, which is the record of a shaft sunk at a distant local-
ity in the same basin, we have only the upper bed of coal at the
base. The two sections give a pretty clear idea of the strata which
include the two lower beds of coal. Above the coal-bearing portion, there
is an interval which we estimated at about 200 feet, in which the beds
were obscure, but thin seams of impure coal cropped out. The mate-
rials were clays, arenaceous clays, and thin layers of sandstone, yield-
ing 80 readily to atmospheric forces that no sharp blufts are formed, so
that the character of the strata could not be clearly seen. We then
bave a range of high bluffs 200 to 400 feet high, which begin at the base
of the mountains, about two miles north of Manitou, and extend across
Monument Creek, and reach off to the southeast far beyond the limitNof
rision, down the entire valley of the Fountain to its entrance into the
Arkansas River near Pueblo. The rocks all around Pueblo are Creta-
ceons, yet it is quite possible that far to the eastward the Lignitic group
overlaps thera, having originally been connected with the coal-basin to
the south near Canon City. We may thus obtain a dim conception of
32 GEOLOGICAL SURVEY OF THE TERRITORIES.
tbe vast erosion that most have taken place here, to have removed H
great a thickness of strata from so vast an area.
The bhiffs east of Colorado Springs, above that portion shown in See
tions a and 6, may be regarded as barren of workable beds of coal, i^l
detailed section of the beds was taken, but it seems hardly necessai;^ \
to present it here. So variable are these beds that the sections witbit
a fourth of a mile would only bear a general resemblance to each othei^
Tbe beds are made up of alternate layers of clay and sand, with irregu^
lar beds of concretionary sandstone throughout. Tbese beds of sau^V'
stotie change constantly, sometimes 30 feet in thickness, and quite ma|\\^
sive at one point, and within a fourth of a mile either thinning out
changed into soft or indurated sand. Toward the summit of the blul
is a thick bed of rusty-brown sandstone, which has been worn by
atmosphere into remarkably rugged forms. As .we proceed northwi
from Colorado Springs to the source of Monument Greek, on the divi<
between the South Platte and tbe Arkansas drainage, the upper b<
of the Lignitic group appear entirely destitute of coal, with a vast thi<
uess, estimated at 1,500 to 2,000 feet, with unusually coarse sediment
The materials composing these Upper Lignitic strata of the Monume|
Creek present the appearance of having been deposited with nnusi
rapidity in moving or disturbed waters. Figures show with grei
clearness this peculiar character of tbe sediments. The peculiar groQ
of strata which, in 1869, 1 called tbe Monument Creek group, extends t
a point within about twenty miles of Denver, where the Lignitic sell
ments return tx) their usual character, and then continue north wat
nearly to Cheyenne.
For a distance of about thirty miles north of west of Monument Creel
the coarse variegated sandstones of the Monument Creek group lap d
to the granites, have been slightly elevated so a^ to incline 5^ to 1^
but not detached from the granites, so that for a considerable distant
tbese granite foot hills formed tbe western shore-line for the great lal
This group is more fully treated in a subsequent portion of this chi
ter.
Up to the present time, but few invertebrate remains have been foui
in tbe Lignitic group from the Arkansas to Denver; but in tbe loWT^^^
strata in the vicinity of the coal-beds a number of plants have hei
observed, belonging in most instances to well-known species occurrioi
elsewhere. These plants were observed by tbe Survey in several Io<
ties along the southern border of tbe groui), generally in tbe bed of sai
stone immediately below tbe lowest coal, and ranging up 100 to 150 U
The species, as identifled by Lesquereux, are Sahal Campbelli, Plata\
Haydenij Ficus tillccfolia^ Domheyopsis obtusa. Tbe &abal has hi
found at Raton Hills, Golden City, Black Buttes, and on tbe Up]
Missouri River near Fort Union. Tbe riatamis occurs at Kat
Hills, Golden City, Black Buttes, and was originally described from
Upper Missouri River, where it is found in great numbers. Tbe Fu
has been obtained from Evanston on tbe Union Pacific Railroad, Kat
Hills, and in Montana on the Yellowstone, so that tbe evidence, so
as it can be derived from the few vegetable remains, connects this groi
witb the RatOQ Hills group to the southward, and far to tbe north t
tbe Upper Missouri. Other species have been identified. .
From Colorado Springs, we may follow tbe Lignitic group northwal
very nearly to Cbeyenue without any break. For a short distance, i
we bave previously remarked, tbe Monument Creek group laps on to tl
granites, entirely concealing all older formations; but very soon afti
crossing tbe "divide'' to tbe drainage of Plum Creek, tbe older beds t
\CdixZ outcrxjp'\
rr~r s
pft*"'^^^
V f V (
'"/•l- »
HATDES.J GEOLOGY — ^LIGNITIC GROUP — SECTIONS. 33
appear in the form of uplifted ridges. This belt, though varying much
in width, is not again interrupted until we reach a point within a few
miles of the Union Pacific Railroad, west of Cheyenne. Sometimes this
belt extends out from the mountain foot-hills four or five miles, and
again it closes up so that the Lignitic bed, as at Golden City, extends
Dp to within one-fourth or one-half a mile of the granites.
I need not describe again the geological features of the district about
Golden City, so much has already been written, nor need I reiieat the
fifty or sixty species of fossil plants which have already been detected
in this far-famed locality. On the map which accompanies this report,
the boundary-line between the Lignitic group and the well-marked Cre-
taceous strata is shown very clearly. We may say that very soon after
leaving the granite foot-hills, the Lignitic beds, at whatever angle they
may be found to incline, return to a nearly or quite horizontal position.
We may say that they incline at all angles from 5^ to 70^, depending
apon their distance from the base of the mountains.
From Colorado Springs to Golden City, the outcrops of the coal are
very rare; but, from Golden City to the Big Boulder, they are quite com-
mon, and the most productive coal-mines in Colorado are found there.
That beds of lignite or coal underlie the plain country far to the east,
there is hardly room to doubt. About ten miles east of Denver, on the
Kansas Pacific Eailroad, at a locality called Tousland. several shafts
have been snnk in the level prairie, and a thick bed oi coal or lignite
was found at moderate depths.
A section of the strata is as follows : —
1. Cltty, gravel, etc
t Soft sand-rock 10 to 12 feet.
3L Sandstone, with seams of coal varying from 1 to 18 inches in thickness,
with 6 to 8 inches of sandstone between 30 feet
i Coal, or lignite • 6 feet.
h. Sandstone, forming the floor of the mine.
This is one of the most elaborately and elegantly prepared mines in
Colorado Territory ; but the coal contains so large a percentage of vol-
atile matter that it will probably not be made available for economical
purposes until the more valuable coal-mines in the vicinity are ex-
haosted. The great scarcity of timber all over this portion of the West
nay, at some future day, render any kind of combustible material val-
oable as a fuel. One shaft sunk here is 245 feet deep, and a second one,
aboQt a mile distant, is 145 feet deep. Both of them passed through
this 6-foot bed. The strata are horizontal. This bed is probably higher
vp in the series than any of the beds that are wrought near the base of
the mountains. A few impressions of deciduous leaves were observed
' !re, but no other fossils of any kind.
Again, near Platteville, on the line of the Denver Pacific Eailroad,
h of Denver, we find that several shafts have been sunk for coal
r the outer border of the group. About a mile south of Platteville,
shaft was sunk 32 feet through the following strata, descending : —
Cby 8 feet.
Seson of iropnre coal 1 foot 6 inches.
Htrd sandstone 10 feet.
liBloe qoartzitic sandstone 1 foot 2inches.
' Black oarbonaceons clay, as roofing 5 feet.
Coal 2 feet.
Black clay, as a floor.
The Hopkins mine is about a mile and a half east of Stoner's. Here
shaft was sunk 05 feet. The mine is now abandoned. About two
3 H
,'
34 QEOLOaiCAL SURVEY OF THE TERRITORIES.
miles northeast of Platteville, two iudostrious miocrR have sunk shafts
in two places. The first one passes through the following beds, from
the surface: —
1. Yellow sand-clay 42 feet.
2. Clay or soapstoue, with 3 inobes of a black material and called by the min-
enismat 2 feet.
3. Clay 4 feet.
4. Abedofahells 3i feet.
5. Clay 6 inches.
6. Durk Baud H f^^*
7. Sandstone, yellow and gray 10 feet.
8. Clay 4 feet.
9. Coal 2i feet.
10. Clay-Ehale. 4 inches.
11. Finesaudyclay 2 feet
12. Coal.
Forty- eight feet from the surface, the workmen came to a remarkable
bed of shells. Masses were thrown out upon the surface 18 inches in
thickness, a mere aggregate of shells. Anomiaj and the same species
of cy renoid or brackish-water shells, found over a workable bed of coal
at Hallville, on the Union Pacific Bailroad, have been identified. About
300 yards from the last shaft, a second one was sunk 53 feet, passing
through a bed of coal 29 inches thick, which is being wrought with great
industry and some profit. These mines are just on the east border of the
South Platte, while on the west side the Upper Cretaceous beds are exposed.
Thin remnants of the Lignitic strata may occur on the west side, but no
Irace of coal in that immediate vicinity. We may, therefore, reason-
ably infer that this thin bed of coal near Platteville lies very near die
base of the Lignitic series.
The next locality which we may mention is still farther to the north-
ward, about ten miles to the northeast of Oreeley, called Higley's mine,
on section 20, township 6, range G6. The mine is opened in the levtl
prairie, thirty miles east of the base of the mountains. The shaft passes
through horizontal layers as follows : —
1. Arenaceous clay.
2. Hard bluish quartzitic sandstone 2 feet.
3. Clay 4ifeet.
4. Coal S^feet.
5. Floor of sandstone.
A few fragments of leaves were observed in the hard sandstone, but
no other fossils. Shafts have been sunk in many other places east of
Greeley, but only thin beds of rather poor coal were detected. It is not
probable that any valuable beds of coal will ever be discovered in the
immediate vicinity.
Our examinations of the country between the South Platte and the
base of the mountains, especially along the valley of the Cache h la
Poudre, were productive of most important results. We found in an
extensive series of sandstones, sands, clays, etc., a great variety of marine
invertebrate fossils belonging to well-known Cretaceous types. The
rocks are all quite peculiar, indicating by their structure that these dep-
ositions took place in moving waters. A few of the shells were found
in the clays, and many of them were inclosed in dark, round, calcareous
concretions, scattered through the clay ; but most of them occur in
isolated grou[>8 on the under or upper surface of a layer of sandstone, as
if they had been swept into eddies or shallow depressions. As we have
often stated, the physical history of these massive formations is written
on the rocks themselves.
Table Suite capped icitfi Trachyte
5 milee north of the Arkansas
and Plaite River divide.
fal Sandstone. I bb I Fire clay. f9&\ Lignite.
Deposit of Lignite in an irregttlar cavity
in sandstone
HATDui.) GEOLOGY — ^FOX HILLS GROUP. 35
In the lower portion of Cretaceous No. 6, or the Fox Hills gronp, the
sediments all show a moderately deep sea and quiet waters, in which
the various forms of MoUusca peculiar to this group flourished in great
abundance, and have been preserved with wonderful perfection. But as
we pass upward, we begin to observe signs of a gradual change to shal-
low and even turbulent waters. Tracks and trails of worms, etc., are
seen on the surface of the thin layers of sandstone, and the more mass-
ive sandstones become concretionary, irregular, sometimes quite thick,
and then suddenly thinning out so as to be unimportant or entirely
absent. While many of the species peculiar to No. 4 as well as No. 5
continue to flourish to a certain extent, new forms are introduced, such
as Tancredia americanay Gardium specwaum^ Mactra fonnoaay Mactra altay
and many others, previously known to occur in no other locality in this
country except near the mouth of the Judith Biver on the Upper Mis-
souri. There are also mingled with them Baculites^ Ammonites^ Inoce-
ramuSy etc., forms well known in the Fox Hills group all over the West.
We may continue our way northward to Oheyenne, and from thence to
the Missouri and the Yellowstone region to the north line of the United
States, and we shall And the Lignitic group remaining substantially (he
same and bearing similar relations to the Fox Hills group below. In
all this distance, the only break in the connection that occurs is a dis-
tance of about two hundred miles, between Oheyenne and the North
Platte, where the Lignitic group is overlapped by the more modern beds
of the White Biver group.
Our investigations in Colorado seem to warrant the following conclu-
sions : —
Ist. That through the upper portion of the Fox Hills group, there are
clear proofs of a radical physical change, though very gradual, usually
with no break in the sequence of time. In this portion of the group are
well-marked Cretaceous fossils of purely marine types, and no others.
2d. That above the upper Fox Hills group, there are about 200 feet of
barren beds, which may be regarded as beds of passage to the Lignitic
group, which more properly belong with the Fox Hills group below. In
this group of transition beds, all trace of the abundant invertebrate life
of the great Cretaceous series below has disappeared.
3d. In almost all cases we find at the base of the true Lignitic group
a bed of sandstone, very irregular in thickness and structure, which
seems to mark the horizon or dawn of this group. In this sandstone,
the first deciduous leaves peculiar to this group occur. No purely ma-
rine Mollusca pass above this horizon. Estuary or brackish-water shells
are found in many localities in great abundance. These soon disappear,
and are succeeded farther north by fossils of purely fresh-water origin.
Whatever view we may take in regard to the age of the Lignitic group,
we may certainly claim that it forms one of the time-boundaries in the
geological history of our western continent. It may matter little whether
we call it Upper Cretaceous or Lower Eocene, so far as the final iiesult
isconcerned. Weknow that it playsanimportant,and,toacertain extent,
an independent part in the physical history of the growth of the conti-
nent. Even the vertebrate-paleontologists, who pronounce with great
positiveness the Cretaceous age of the Lignitic group, do not claim that
a single species of vertebrate animal passes above the horizon I have
defined from the well-marked Cretaceous group below.
Having presented these facts as briefly and clearly as we were able,
we will leave the further discussion of the age of the group to a future
period.
36 GEOLOGICAL SURVEY OF THE TERRITORIES.
MONUMENT GREEK GROUP.
On the bigh divide between the drainage of the Arkansas and South
Platte Rivers, we find a somewhat singular formation, differing in some
respects from any other that we have met with in the West. The sedi-
ments were undoubtedly deposited in a rather modern fresh-water lake ;
but whether we can synchrouize this group with any of the other lake-
deposits in the West remains yet to be discovered.
This group was named by me in 1869 the Monument Greek group,
from the fact that the atmospheric agents have carved out of some of
the beds a very peculiar kind of monument, or columns, which long ago
attracted the special attention of the traveler. These columns have
given name to a small stream, which rises in the divide, and flows south
into Fountain Creek, also to a very interesting locality now known as
Monunient Park, in the valley of West Monument Creek, where these
singularly-shapecl columns do most abound. These singular columns
have been frequently described in previous reports of the Survey ; but
the accompanying figures on Plate 3 presents them to the eye in their
varied forms far more clearly than any description in words.
'The boundaries of this basin have not yet been detern^ined, but it is
believed that it does not occupy a very large area, probably confined to
the high ridge or divide which seems to give origin to so many small
streams, which, as seen on the map, flow south into the Arkansas River.
In this basin, Beaver, Kiowa, Bijou, Box Elder, and Cherry Creeks,
branches of the South Platte, take their rise ; while to the south, many
branches of the Fountain and Chico take their origin, and flow far south-
ward into the Arkansas. With our present knowledge, we may estimate
the area approximately as about forty miles from north to south and fifty
from west to east, or about two thousi nd square miles. It is plain that
it originally extended over a much larger area ; the evidences of denuda-
tion by which large portions have been removed being apparent all
around its borders. The basin itself lies in the Liguitic group. All
around its south, north, and east borders, we find the beds of this group
cropping out, while on the west side they are exposed, when not con-
cealed by the nearly horizontal beds of the more modern group. Except
along the base of the mountains, it is not easy to detect any want of
conformability in the connection of the two groups ; and this relation is
obscure, when the older beds are lifted up at the base of the granite
hills, on account of the great amount of local drift, which seems to cover
everything to a considerable thickness.
The texture of the rocks of this group is quite varied. The aggre-
gate thickness is probably about one thousand five hundred feet. The
lower portion is composed of rather massive beds of sandstone, varying
from a puddingstone to a fine-grained sandstone, usually of a light color,
sometimes yellow or iron-rust, with their intercalations of arenaceous
clay. In the distance, the whole group presents a chalky- white appear-
ance in many localities. At the immediate base of the mountains, just,
south of the small lake on the divide, the rocks are variegated sandstones,
brick-red, white, and yellow, varying in texture from a fine sandstone to
a puddingstone, with all the signs of deposition in moving waters, and
so closely resembling the older red sandstones, which we had u^^ually
regarded as Triassic, that I had no small difficulty in determining their
exact position. Still farther north, on the divide proper, the beds jut
against the granites, inclining not more than 3^, and are made up of a
coarse aggregate of feldspar and quartz crystals, so that it resembles a
very coarse granite. It is plain that the sediments of this group were
■Library.
X^U'CM
36 GEOLOGICAL SURVEY OF THE TERRITORIES.
MONUMENT OBEEK GROUP.
On the bigh divide between tbe drainage of tbe Arkansas and Sonth
Platte Bivers, we find a somewbat singular formation, differing in some
respects from any otber tbat we bave met with iu tbe West. Tbe sedi-
ments were undoubtedly deposited in a ratber modern fresb-water lake ;
but wbetber we can syncbrouize tbis group witb any of tbe otber lake-
deposits in tbe West remains yet to be discovered.
Tbis group was named by me in 1869 tbe Monument Greek group,
from tbe fact tbat tbe atmospberic agents bave carved out of some of
tbe beds a very peculiar kind of monument, or columns, wbicb long ago
attracted tbe special attention of tbe traveler. Tbese columns bave
given name to a small stream, wbicb rises in tbe divide, and flows south
into Fountain Creek, also to a very interesting locality now knowu as
Monument Park, in tbe valley of West Monument Creek, wbere these
singularly-sbaped columns do most abound. Tbese singular columns
bave been frequently described in previous reports of tbe Survey ; but
tbe accompanying figures on Plate 3 presents tbem to tbe eye in tbeir
varied forms far more clearly tban any description in words.
*Tbe boundaries of tbis basin bave not yet been detern^ined, but it is
believed tbat it does not occupy a very large area, probably confined to
tbe bigb ridge or divide wbicb seems to give ori^rin to so many small
streams, wbicb, as seen on tbe map, flow soutb into the Arkansas River.
In tbis basin, Beaver, Kiowa, Bijou, Box Elder, and Cberry Creeks,
brancbes of tbe Soutb Platte, take tbeir rise ; wbile to tbe soutb, many
branches of tbe Fountain aud Cbico take tbeir origin, and flow far south-
ward into tbe Arkansas. Witb our present knowledge, we may estimate
tbe area approximately as about forty miles from north to soutb and fifty
from west to east, or about two tbousi nd square miles. It is plain tbat
it originally extended over a much larger area ; tbe evidences of denuda-
tion by wbicb large portions bave been removed being apparent all
around its borders. Tbe basin itself lies in tbe Liguitic group. All
around its soutb, north, and east borders, we find tbe beds of tbis group
cropping out, wbile on the west side they are exposed, when not con-
cealed by tbe nearly horizontal beds of tbe more modern group. Except
along the base of the mountains, it is not easy to detect any want of
conformability in tbe connection of tbe two groups ; and tbis relation is
obscure, when tbe older beds are lifted up at the base of tbe granite
bills, on account of tbe great amount of local drift, wbicb seems to cover
everything to a considerable thickness.
Tbe texture of the rocks of tbis group is quite varied. The aggre-
gate thickness is probably about one thousand five hundred feet. The
lower portion is composed of rather massive beds of sandstone, varying
from a puddingstone to a fine-grained sandstone, usually of a ligbt color,
sometimes yellow or iron-rust, witb their intercalations of arenaceous
clay. In the distance, tbe whole group presents a chalky- white appear-
ance in many localities. At tbe immediate base of the mountains, just,
south of the small lake on tbe divide, tbe rocks are variegated sandstones,
brick-red, white, and yellow, varying in texture from a fine sandstone to
a puddingstone, witb all tbe signs of deposition in moving waters, and
so closely resembling the older red sandstones, which we bad usually
regarded as Triassic, tbat I bad no small difiSculty in determining their
exact position. Still farther north, on tbe divide proper, the beds jut
against the granites, inclining not more tban o^j and are made up of a
coarse aggregate of feldspar and quartz crystals, so tbat it resembles a
very coarse granite. It is plain tbat tbe sediments of tbis group were
Library.
J" CM
HAYDBs.] GEOLOGY ^aiONUMENT CREEK GROUP. 37
derived very largely from tbe granitoid rocks. The sediments become
finer and finer as we recede eastward from tbe foot of tiie mountains
into the plains.
To the eastward of tbe line of tbe Denver and Eio Grande Railroad,
tbe surface is cut up into more or less rectangular masses, with rather
broad table-shaped summits, varying from four hundred to eight hun-
dred fe^t in height. Tbe sides are often very steep — almost inaccessible.
At a remote period in tbe past, tbe erosion has been very great, carving
oat by an almost inappreciably slow process, these broad valleys, leaving
these buttes here and there, composed of horizontal beds, to aid in form-
ing some conception of tbe amount of denudation wbicb has taken place.
It is not possible at the present time to estimate tbe original thickness
of this group, but we believe it to have been very much greater than
the highest beds now existing would indicate. The summits of many
of these buttes are capped with a greater or less thickness of sKbeautiful
purplish trachyte, wbicb must have ascended in the form of dikes from
beneath and flowed over the surface. Much of tbe trachyte is a sort of
breccia, composed of rather coarse sandstones, wbicb must have been
caught in tbe melted material. It is quite evident that these outdo ws
occurred during tbe existence of tbe lake, though at a late period. As to
tbe real age of this group, I am inclined to regard it as Miocene, perhaps
Upper Miocene. The great Front or Colorado range was elevated much
as it is at present, though it rose some hundreds of feet during and per-
haps since its deposition. Some of tbe lower beds of tbe group, though I
jutting up against tbe granitic mountain-sides, have evid^^ntly been ^
lifted up several hundred feet above tbe same strata, far east on the
plains. I think it might be synchronized with tbe upper portion of
the White River group far to the northward, and is probably of the
same age as tbe fresh-water deposits in the South Park, just over
tbe range, wbicb have yielded such an abundance of fossil leaves of
plants, fishes, and insects. Up to tbis time, tbe Monument Creek group
has yielded but few fossils, and those are vertebrates. Professor Cope
states that, in tbe summer of 1873, be made a brief examination of this
group for vertebrate remains, and be states that be discovered tbe bind
leg and foot of an Artiodactyle of tbe Oreodon type. He also has every
reason for believing that tbe fragment Magaceratops coloradoensis came
originally from tbe same locality. He further believes the group to be
of Miocene age, which was tbe conclusion of the writer in 18G9. Pro-
fessor Cope is disposed to regard tbe fresh water strata in tbe South
Park as newer than Eocene and probably Miocene.
I see no reason why they should not be of tbe same age as tbe Monu-
ment Creek group. Tbe strata are horizontal, or nearly so, and bold
about the same position in relation to tbe granitic rocks in the vicinity
as the Monument Creek group. Tbe sediments are quite difierent, it is
true, and the fossil remains most abundant and varied in character.
This condition might very well exist, inasmuch as we may suppose that
the Front range entirely shut off all connection between them. Vol-
canic action seems to have been going on to a great extent during tbe
deposition of tbe South Park beds, and a great portion of tbe sediments
is composed of tbe eroded material of tbe igneous rocks.
38 GEOLOGICAL SUBVET OF THE TEBRITOBIES.
APPENDI3J: TO CHAPTER II.
By H. T. Wkst.
Different strata passed through in horing for an artesian well by H. T,
West^ on section 32, township 5 norths of range 66 west^ being in ike
county of Weld^ in tJie Territory of Colorado — bore^ 3 inches in diameter.
Feet In.
Stirfaoe-Boil 22 0
White sand-rook ^ 7 0
Bluesbale 7 0
Black shale 2 6
Coal 0 6
Brown rock 8 0
Hard browo rock (sandstone) 2 0
Brown rock 13 0
Hard brown rock 1 0
Soft brown rock 8 0
Blue shale 5 0
Hard white sand-rock 2 0
Blneshale 7 0
Hard blue shale 2 0
Blneshale 8 0
Hard blneshale 3 0
Blneshale 4 0
Hard blneshale 3 0
Bine shale - 10 0
Rock 1 %
Blue shale 5 0
Hard blue rock 1 0
Bluoshale ', 3 0
Rock 3 0
Ruck (probably of a different character) 5 0
Hard rock 3 0
Bine shale 3 0
White rock 3 0
Gi ay rock 4 0
Blneshale 2 0
Hard rock 3 0
Orayslate 4 0
B.ue slate 2 0
Orayslate •.. 3 0
Rock 2 0
Blneshale 3 0
Hard slate ; (I am doubtful may have been coal) 4 9
White sand-rock 5 0
Hard white sand-rock 3 0
Blue shale 1 4 0
Hard blneshale 2 0
Hard shale 3 0
Hard blue rook 5 0
Blneshale 1 0
192 0
These mem.oranda were taken from the book kept by the man who
did the boring. He saved samples of each stratum, bat I think that
they have been destroyed.
Higley's coal-mine is in section 20^ township 7 north, of range
66 west. Mr. La Grange prospected for a company, of which I was the
secretary, in sections 17 and 22, in the same township and range. He
made a rough diagram of the results of his drilling (boring), which I
have sent him, witli the request that he perfect it and return to me, an4
when he does so I will dispatch it to you.
GEOLOGY — STRATA.
39
By the minntes which I kept, I find that he made a verbal report as
follows, Janaary 23, 1871 : —
Hr. La Grange made a report of his operations in sections 17 and 22, with a rongl^ dia-
gram of his, views in rec^anl to the difterent strata of coal in these sections; also that
tbe thickest vein of coal through which the drill had passed in horing in section 22
was 2 feet 7 inches. *
Od the 8th of Febraary, 1871, he further reported —
That he had put down a series of horings in different sections to determine whether
tbere were any large veins of coal to he foand, and that he could find nothing thicker
tban three feet, the veins found varying from one to three feet.
That horing to the eant of section 17, on section 22, he struck and passed through
six different veins, none over 2^ feet thick.
He also stated —
That the coal seemed wfter than that found on section 17.
That, in accordance with instructions, he had hored 51 feet on a section to the
soatbeast, finding five different veins of coal, the lowest being the thickest, and that
^ feet thick and softer than in section 17.
That he had also prospected to the west of the shaft sunk by our company on sec-
tion 17, finding, at a depth of 27^ feet from the surface, a vein of good hard (for soft
coal) coal; and further prospecting seemed to determine the fact of a rise in said vein
to the west of two inches to the rod.
He farther stated —
That be had thought it best, before cntting an incline (to shaft on section 17), to
test the character of the coal and the profitableness of working it, by chambering,
trhich had developed an inclination, or dip, eight inches in ten feet, which allowed
tbe water to follow the work, thus rendering this mine nnprofitable.
There seems to have been some convulsion of nature in that town-
ship, as will be seen from the fact that the Higley vein pitches in such
a way as to drain the mine, while at our shaft^ not forty rods north, it
dips as stated.
CHAPTER III
Rksum]^ of the Geology along the Eastern Base of the Front or Colorado
Range: Silurian, Carboniferous, Triassic, Jurassic, and Cretaceous Groups.
The various groups of sedimentary rocks that occur aloug the eastern
slope of the Front Eange of Colorado from Canon City to Cheyenne
have been so often described in previous reports that it seems hardly
possible to add anything further of importance. We will be able, there-
fore, to do little more in this connection than to describe, with some cara.
the maps, sections, and other illustrations which we have prepared I
this report.
The '* Preliminary map of the eastern base of the Rocky Mountaim
will be found to explain itself to a great extent. The topogi*aphy
given with much detail and in a picturesque form, so that the relatiol
of the sedimentary to the granitic rocks are admirably presented. tA
characteristic forms of the *'Hog Back'' ridges which have been]
often noticed, is clearly shown, as well as the en Mielmi features of (4
minor mountain-ranges as they run out into the plains.
The pictorial sections which accompany the map will serve to sh
more dearly than we have hitherto done what we have denomina
the plain and mountain districts, as well as the abrupt transition fr<
one to the other. The plain country extends uninterruptedly from tl
Missouri Kiver to the base of the mountains. The elevation abo4
sea-level at Kansas City is 764 feet; at Denver, by way of the railroi
639 miles to the westward, the elevation is 5,197 feet ; showing an avel
age ascent of about seven (7) feet per mile over an apparently levi
treeless plain. Over this broad space the strata are very nearly
quite horizontal in position, until within a few miles of the mountain!
where they are lifted up at various angles and the mountain-raug(
seem to rise abruptly out of the plains. The topography as well as th(
geology of the plain country is remarkably simple, and' it is only in
narrow belt along the immediate foot of the mountains that it becom<
more varied and complex. The elevation of the great Front or Colorado^
range carried up the sedimentary formations which originally rested oai
its sides or summit, and the uplift seems to have been very nearly 6r|
quite vertical. Whether these formations originally extended uniuter-f
ruptedly across the area now occupied by the mountain-ranges, is 2k.
question which will be more fully discussed at some future period. That
this was the case in part, I am very confident, but there are facts that
appear to disprove this statement in some instances. It seems proba-
ble that a portion of the Bocky Mountain range was outlined at an !
early period; that it has grown, as it were, through successive ages up
to the present time. A careful examination of the map and the picto-
rial sections will enable the reader to understand more clearly the
remarkable belt of uplifted sedimentary beds along the immediate base
of the mountains. Although they seem to be more interesting and
picturesque in Colorado, yet these ridges occur to a greater or less
4D
}i^S
i-ry
r
r
iL-
I'iG. 1.— Nmim.E-RucK, Gles liYKiii, Kko TiUAiiitio Sandstosk.
Fio. 8.— CoMCBBTJOse AND Sandstonks, Ckbtackous Pbkmi
PUte V.
Fig. 1.
-..•AiftS^
o/
Showing the changes in the sediments as we approach
the granite ''shore lineS' At the line a,the frag7nents are large
and unworn. Farther out they are more rounded and have
a matrix of pebbles and sand. Between the lities aa,
and bb, there isabelt^that, although probably Sedimentary
can hardly be distinguished from the true granite.
Fig. 2.
I
Thickening of Sedimentary beds along the ** Shore
line"as seen near Manitou.
-J
Fio. 1.— Cross- BBDMMa Liokitic Sindstokes, nbar Cor^-
RADO Sprinoo.
HATDBK.1 GEOLOGY OP COLOBADO SPRINGS AND PLEASANT PARK. 41
extent on both sides of the eastern ranges that front the plains, from
the northern to the southern boandary of the United States, and how
mach farther I do not know. It is probable, however, that thej extend
far north into the British Provinces and far south into Mexico. This
belt is ver^' varied in its character from point to point, sometimes ex-
pands to a width of several miles, and again contracts to a fourth or
half a mile in width. Sometimes a full series of the formations known
in the west, from the older Silurian to the most modern Tertiary, are
clearly exposed, inclining at various angles; and then again only the
more modern beds can be seen. It is on this account that the geology,
though appearing so very simple in its character, is really quite com-
plex when examined in detail.
Up to this time we have determined the existence, in this belt in
Colorado, of the Silurian, Carboniferous, Triassic,(f) Jurassic, Cretaceous,
and Tertiary groups; yet, while the more modern formations are very
persistent throughout the entire distance from the north to the south
line, some of the older beds are wanting in many places. To the far
north, along the margins of the Black Hills, Big Horn, and Wind Kiver
Mountains, the Potsdam sandstones, with perhaps more modern divis-
ions of the Silurian, are well exposed and quite continuous, while to the
southward these rocks disappear, except at restricted localities. We
find near Colorado Springs and Canon City quite large exposures of
Silurian beds, with a few fossils that are allied to those of the Calcifer-
oas group of the Lower Silurian of New York. In the interval, from
Fort Laramie to Colorado Springs, a distance of over 200 miles, no one
connected with the survey under my charge has yet detected luiy trace
of these beds. It is possible that in Pleasant Park, about 50 miles south
of Denver, there are traces of this formation in the variegated sand-
stones that lie next to the granites, as shown in the section. At Color-
ado Spiings, and in the vicinity, there is a considerable thickness of the
Silorian beds, which have been frequently described. The reddish-
brown, rather coarse sandstones at the base, rest upon stratified grani-
toid or gneissic rocks unconformably, as shown in the illustration (PI. YI,
Fig. 2). Above the sandstones there are 600 to 800 leet of yellowish
limestone, which, in some instances, is a reddish color, in which have
been found several species of invertebrate Silurian fossils. South of the
valley of Fountain Creek the uplifted belt rapidly closes up to the base
of the mountains, and for some distance no beds older than the Creta-
ceous are visible. From Fountain Creek to Canon City this belt ex-
pands and contracts from time to time, so that it is quite possible that
small isolated patches of the Silurian group may appear in a few places.
At Canon City, and resting for the most part on the mountain-sides, in-
etining at a high angle, there is an extensive thickness of these older
beds again. The lower portion is a variegated micaceous, slightly cal-
careous, sandstone, closely resembling, in texture and composition, the
Potsdam sandstone as seen in other localities further to the north.
Some tolerably well-defined fossils were discovered in the sandstone
which rests directly on the granitic rocks, which Mr. Meek has pro-
noQDced of undoubted Lower Silurian age, but they have not yet been
described. This sandstone passes up into a hard and rather massive
limestone, evidently the same as that noted at Colorado Springs.
We cannot say more at present in regard to rocks of this age, than
to state our belief that they underlie the entire country along the east-
9TU slope of the Rocky Mountains, from our northern boundary to New
Mexico, and that, where they are not visible, they may possibly be con-
cealed by tho overlying and more modem beds.
42 GEOLOGICAL SURVEY OF THE TEBBITOKIES.
THE carboniferous' GBOTJP.
The GarboDiferons g^oap is a little more persistent, and yet tbis seems
to be wanting over extended intervals, unless a portion of what have
been called the Bed Beds is of this age. This group is exten-
sively exposed along the flanks of the mountains, 100 to 150 miles
north of Cheyenne, as was shown in the annual report of 1870. It
seems, however, to diminish somewhat in force, and to contain
comparatively few fossils in its southern extension, until we reach
Canon City. From thence southward into New Mexico it increases
again in thickness and importance, and yields an abundant supply of
its characteristic fossils. I have no positive information of the dis-
covery of any well-marked Carboniferous fossils from the line of the
Union Pacific Eailroad to the vicinity of Canon City, although strata
supposed to be of that age are exposed in a few localities. On the
small map of ^'Colorado Springs and vicinity," a light band will be
seen between the Silurian on the west and the Bed Beds or Triassic on
the east, which represents a peculiar group of strata not observed else-
where on the eastern slope, but resembling v6ry closely a series of varie-
gated beds, described by Dr. Peale, in the annual report for 1873, in
the valley of Eagle Biver, which yielded well-marked Carboniferous
types. This group of strata is composed of variegated beds of sand-
stones of various textures, alternately with layers of arenaceous clay.
The entire thickness was estimated at about 1,000 feet. It is most
probable that these beds are of Carboniferous age.
From Colorado Springs the Carboniferous group is not conspicaons
at any locality, and for a great portion of the way is not seen at all, but
at Canon City and Wet Mountain Valley the limestones and sandstones
contain numerous fossils, both animal and vegetable. From the Wet
Mountain Valley, which is but a short distance south of Canon City,
Mr. B. N. Clark collected specimens of vegetable remains from the Car-
boniferous beds, which were submitted to Professor Lesquereux. He
detected Sti^ariafucoides, Brgt., showing scars of surface with stems
and leaves attached ; mold of the internal surface of the cylinder of a
Calumites ; small specimens ot a new species of GordaiteSy resembling by
its nervation Vordaites prifidpalis. An abundance of invertebrate fos-
sils have been discovered in this group which have not yet been studied.
THE BED BEDS OB TRIASSIC OROUP.
The Bed Beds or Triassic group is very persistent, and if absent at all,
only at very short intervals. No organic remains have yet been found
in this group by the members of the survey under my charge, yet, for
various reasons, we have assumed the red sandstones to be of Triassic
age. It is barely possible that a portion or all of the group is of Juras-
sic age. Yet Professor Cope is of the opinion that he has discovered
evidence in New Mexico of its Triassic age. The history of this group
is still obscure, and remains as one of the problems to be solv^ by
more extended and more thorough explorations. Geographically, it is
one of the most widely distributed formations in the West. From the
northern boundary to the southern line and east of the Wasatch range
in Utah, this red formation makes its appearance wherever a mountain-
range is elevated so as to expose the various sedimentary groups. The
evidence indicates that it extends without any important interruption
over the broad area as defined above. This group is generally admitted
to be in part, or entirely, of Triassic age, and I have always so regarded
?5 3
#11
.''U' •>.
■■' -" *• >.-
if • \
/■
t
!
Sandstoneh,
KATDMH.] CURIOUSLY-ERODED SANDSTONES. 43
it, since my first examination of it, nearly twenty years ago, yet more
direct proof mast be brought to bear before long in some portion of our
continent. These red sandstones have always attracted much attention
wherever noticed, on account of their peculiar color, but nowhere have I
ever observed them performing such a conspicuous part in giving form
to the scenery of the country, as along the eastern base of the Bocky
Mountains in Colorado. This feature is more marked from a point about
fifty miles north of Denver to Golorado Springs, than in any other por-
tion of the continent. Along this belt the sandstones are more compact,
with every variety of red, from a pale dull tint to a deep purple color.
There is also every variety of texture, from a rather coarse conglomerate
to a fine sandstone. It varies much in thickness, ranging from 400 to
2,000 feet. Its greatest thickness south of Platte Canon is in Pleasant
Park and in the '^Garden of the Gods," at Manitou. At Pleasant Park,
according to Dr. Peale, the aggregate thickness of the Red Beds is about
2,000 feet. This series of beds is well shown in the pictorial section.
These sandstones have been elevated at various angles varying from 20^
to a vertical position. In the vicinity of the Manitou Springs, in what
is usually called the ^^ Garden of the Gods," the same variation is seen,
but in many instances the beds are very massive, thick, and stand in a
nearly vertical position. In Plates VIII and IX we can see the massive
sandstones, which have been weathered into the most fantastic shapes,
standing up in immense walls or columns 50 to 250 feet in height.
Plate VIII represents what is called the gate or entrance to the ^^ Garden
of the Gods." In the foreground is seen the massive wall of red sand-
stone rising on either side of the opening to the height of 100 to 150
feet. The wall was originally continuous, but has been worn through by
erosion. Whatever may have been the agents which in times past
have wrought oiit all these remarkable forms, it is piain that they have
acted in former times with far more intensity than at present. In the
background, through the opening, may be seen the snow-capped sum-
mits of Pike's Peak, rising to a height of 14,147 feet above sea-level.
Plate IX gives an example of what might be called a magnificent mono-
lith. It is an immense column of bright-red Triassic (f ) sandstone rising
to a height of 250 feet above the general level, a portion of a massive
stratum elevated to a vertical position, and the contiguous portions
eroded away. Figure 1, plate IX, illustrates the singular columns which
stand at the entrance of the <' Little Garden of the Gods," or, as it is now
called, '^ Glen Eyerie." On account of the peculiar forms which these red
sandstones havereceived from the eroding agents of nature, this locality
will always remain one of the most celebrated in Colorado. *
The more careful study of the relations of these sandstones to the
underlying rocks, has thrown much light on the physical history of
this region. My own observations, farther to the northward, led me to
the belief that the great upHft of the mountain-ranges, though imper-
ceptibly slow, was an unit in its action; or, in other words, that the
changes in the position of all the groups were brought about by the
same cause and at the same time. There could not be a strict conform-
ity in the sedimentary groups, inasmuch as entire groups are wanting,
and in some cases only fragments of others are remaining. But I have
hitherto supposed that the elevation of all the sedimentary strata along
the base of the mountains was a comparatively modern event. We now
have the evidence, from the texture of these red beds and their position
on the underlying granitic rocks, that the Front Range, during the
supposed Triassic period, formed a vast shore-line, and that the sedi-
ments of the Bed Beds were' deposited on the base against the sides of
V
44
GEOLOGICAL SURVEY OF THE TEEBITORIES.
the granitic range. In the annual report for 1873 the fact wai
that the Bed Beds, in the form of coarse conglomerates, filled
uneven surface of the granitic rocks below. South of Mani
find an enormous thickness of very coarse conglomerates, cements
rather fine sands, jutting up against the mountainsides, showing
that, although elevated and disturbed to a certain extent siD<
deposition, they were laid down along the base of the Front Bai
shoreline, and that there must have been a period of compare
pose. When these sandstones, near the base of the mountains, ai
to be made up of conglomerates, they are observed to be very
in the immediate vicinity of the granites, but becoming finer ai
sandstones as they extend eastward into the plains. There shoal
fore be some nonconformity between the Triassic and the Carboi
and Silurian groups below, for both of the latter extend high npi
flanks of the mountains on either side, sometimes occurring on tF
mits of the lower ranges. The section in Plate VII would indicat
thing of this sort, for we find the Silurian and Carboniferous iui
20O and 45°, while the Triassic dips 90^, or is very near a vertical
diagram also shows how the Silurian beds lie high up on the
flanks of the mountains. The elevatory force seems to have act(
ticall}', bending the overlying sedimentary strata like metallic sh<
that within a few yards of the nearly vertical beds the same an
zontal or nearly so. This will explain very clearly the abruptnei
which the mountains seem to rise out of the plains to the trav<
preaching them from the east.
The beautiful pictorial section of Pleasant Park may need a w(
explanation here. The dotted line a a shows that all the eleval
tion in the rear or west of it is composed of granitic rocks. The
line in the foreground, h A, shows the junction of the Lignitic
to the true Cretaceous beds which here rise up in a very narrow
from beneath the Monument Creek group. It is exposed by the;
ing away of the Monument Creek beds. The letter t indicai
usual form and isolated character of the numerous bnttes that ar4
tered over the plains here for a considerable distance east of the
ains. The strata are nearly horizontal, the summits are flat,
shaped, and are not unfrequently capped with trachyte. Betwe<
dotted lines the Carboniferous, Bed Beds (Triassic), Jurassic, an<
taceous groups are exposed. The manner of inclination and tlie
tion of these groups to the granitic range,' as well as to each oti
made clear by the section.
THE JXTRABSIC.
This formation has already been described in so much detail in
vions reports, that I shall mention it very briefly in this couDe<
Far to the north this group holds a prominent position, not only oi
count of its aggregate thickness, but also from the abundance
variety of its organic remains. South of the Union Pacific Bailroa<
Colorado, it is confined to a very narrow belt, with very few if an;
sils to establish its age. That it extends most persistently far s(
ward into New Mexico, there cannot be a doubt. The narrow belt
it occupies is well shown in the small max) ^^ Colorado Springs am
cinity. North of the Pacific Bailroad, along the base of the front n
of mountains, it increases in thickness and is full of characteristic
sils. In the annual report for 1873 and previous reports, the lithol
cal characters of all of these groups have been so fully discussed tl
>N-v.
^cu^yt
roch
■!
jyachytc. J, St4
m
Tocks Test i
I
?K**'»^
library-
^ Of \<^^'^
nAniKc.l THE CRETACEOUS GROUP. 45
would be mere repetition to refer to thein in this report. The Jurassic
group in Colorado has little or no influence economically or in giving
form to the peculiar scenery.
THE CRETACEOUS.
The Dakota group is composed of massive beds of sandstones inter-
sected with layers of clay, and forms some of the most conspicuous
ridges or '* hogbacks" along the eastern base of the Front or Colorado
range. Its importance, however, varies in different localities as much
as its texture ; sometimes it is scarcely seen and then again it forms one
or more of the most important ridges. Its aggregate thickness is
never great, varying from 200 to 400 feet, and may be represented by
a very narrow belt on the map. West of the lOOth meridian it has
yielded very few organic remains, although it has a very extended geo-
graphical range. It is hardly ever wanting along the margins of the
monntain ranges east of the Wasatch Mountains, in Utah. From its
structure in the far West, I regard it as a sort of transitional group be-
tween the well-defined Cretaceous group and the Jurassic below.
Numbers 2, 3 and 4, or the Fort Benton, Niobrara, and Fort Pierre
divisions, may be regarded as one group, under the name of the Colora-
do group, as adopted on Clarence King's beautiful geological map of the
Green River basin. To one who has never studied these divisions in the
Northwest, along the Upper Missouri River, there would seem to be no
occasion for their separation. Having studied these divisions with
much care in their typical localities, along the Missouri River and in
Eastern Kansas and Nebraska, I found very little difficulty in tracing
tbem across the country westward and southward, so far as my explor-
ations have extended. It is very doubtful, however, if any geologist
would have ever separated the Cretaceous beds between the Dakota
and Fox Hills groups into divisions, had they been first studied
in the interior of the continent. The Fox Hills group has a very impor-
tant influence on the physical history of a most important geological
period. It was at the close of this period that one of the most impor-
' tant biological changes occurred in geological history. So far as we
know at the present time, no animal-remains, and very few, if
any, vegetable forms, passed above it. A lew species of plants
probably began their existence in the Upper Cretaceous in the
Fox Hills group and continued on up into the Liguitic group,
where they reached their highest point of development. The gradual
approach of shallow seas is finely shown in the character of the sedi-
ments in the upper portion of the Fox Hills group. Not only the shal-
low seas but the gradual change of salt to brackish and then to purely
fresh waters was amply sufficient to destroy all traces of marine life,
which occur soabundantly in the Fox Hills group. Fig.2, Plate IV, pre-
sents a fine illustration of the remarkable concretionary masses which
cbaracterize iu many localities the upper portion of the Fox Hills
groap as it passes into the brackish-water strata of the Lignitic or
Laramie group above. This cut, though intended to illustrate a portion
of the Dakota group in Eastern Kansas, serves perfectly to explain to
the eye the immense rusty-brown concretions which abound in the mud-
beds just beneath the lower sandstones of the Lignitic group at Canon
City and at Colorado Springs, and at other localities in Eastern Colo-
rado. These concretions are peculiar rounded, regularly stratified
masses, often merely resting upon the pedestals of the softer and
more regularly bedded sandstones below. So far as Colorado is con-
46 GEOLOGICAL SURVEY OF THE TERRITORIES.
cerned, I have observed no locality where there appeared to be any
striking nonconforuiity between the Fox Hills groap and the Lignitic
group above. That there may have been intervals of time, daring
which the (3retaceoas sediments were not deposited ; that there may
have been dry land over large areas, is not impossible, but there could
have been no great degree of erosion of the surface of the upper Cre-
taceous beds. This apparent conformity, while in certain localities
the upper C'retaceous beds received a very much increased thickness,
may be due to a tar more rapid deposition. In almost all cases, the
transition from the Fox Hills group to the brackish- water deposits of
the Lignitic seems to have been gradual, with no visible physical break
of importance. The great break seems to be illustrated only in the
entire change in the animal and vegetable life.
But the time at my disposal will not permit me to discuss here many
important questions in this connection* For the details of the geology
of the Eastern base of the mountains in Colorado, the reader is referred
to the previous annual reports of the survey, especially the one for 1873.
FOUATIUN ov Okanitk i\ Kst
CHAPTER IV
Ancirnt lake basins. — Glacial LAKES.-~MoRAiNAL deposits in the valley of thb
Upper Arkansas River and along both flanks of the Sawatch Mountains.
For Bearly twenty years I have written more or less in regard to the
ancient lake-basius of the West, but it was only within a few years, since
the facilities for traveling have so greatly increased that geologists
have foand that these lake-basins once oocnpied the entire country
from the Arctic Circle to the Isthmns of Darien. In very many in-
stances they were merely expansions of river valleys, like the greater
namber of onr lake-basins of the present day. During the early portion
of the Tertiary period, the western portion of our continent was covered
with immense lakes, some of which occupied a much larger area than
any we are acquainted with at the present time. During the Pliocene
period, and duriog the interval to the present time, thousands of small
lakes, with a few of large size, were distributed over the great area
west of the Mississippi, and the basins with their peculiar deposits are
found in the parks, among the mountains, and along every important
river- valley. The gathering together of the vast afnount of information
which is now accumulating on this subject is a task which will, at no
distant day, be productive of most interesting results.
I have made these few remarks to introduce what I may have to say
in regard to the valley of the Upper Arkansas Biver.
The Arkansas Hiver rises in the Tennessee Pass, nearly west of Mount
Lincoln, in latitude 39^ 2V and longitude 106^ 19', and flows a little east
of south for a distance of about 80 miles in a straight line, when it flexes
to the east, and flows through a deep canon in the granite, and emerges
into the plains near CaOon City. Near the sources of the river are several
expansions of the valley from one to two miles in width, oval-shaped,
and covered with a deposit of drift-material. Near the junction of the
east branch of the Arkansas the valley, with the terraces on either
side, continues pretty regularly about Ave to eight miles in width, but
gradually closes up again below Lake Greek, though on either side are
vast deposits of the coarse drift-material extending high up on the
mountain-aides, especially on the west side of the valley. The valley
then gradually expands out and enlarges about five to ten miles in width
for a distance of nearly 40 miles. In the annual report for 1873 I
have expressed my belief that this valley began in a monoclinal inter-
val, with the great Sawatch range on the west side forming the crest of
the continental water-shed, and the Park range on the east, which,
with its sedimentary rocks and granite basis, formed the east side of a
grand anticlinal, the aggregate mass of rocks inclining to the eastward.
Onr observations over a very extended area only confirmed the opinion
M^pressed in our last report, that the great Sawatch range formed the
central portion of a gigantic anticlinal. The west side of the Park
range is, for the most part, very abrupt, and for long distances the
gneissic rocks show very clearly the direction of the dip. On the east
side the sedimentary rocks dip down under the surface of the South
• 47
I
"T*-
;|i
48 GEOLOGICAL SURVEY OF THE TERRITORIES.
Park. On the west side of the Sawatch range we have the valley of
the Gnnuison, and west of that the sedimentary rocks incline to the
westward, unless disturbed by some center force, for the Elk Mountains.
On either side of the valley small streams flow into the main chaiinel
- « of the Arkansas from the source to Canon City. These streams usually
t"-- have their origin at the very crest or water-divide of the two ranges,
:$r' and in most instances have cut their way through the solid mass to the
-^ 1 * ' m^in river. Many of these streams have numerous side-branches which
-* ' have also carved out wonderful gorges near the crest of the mountains,
t^ ^ giving to these mountain ranges a ruggedness that is almost inconceiv-
. > able to one who has not actually explored them. It is in the study of
t '4 these gorges that the geologist learns to appreciate the immense results
I ' of erosion in giving form to the rocky range of the West. Even yet the
■■ r " power of this force has not been adequately understood, but the wider
i" ■- our range of observation, the greater is our conception of its power.
vj* We may safely assert that at some period comparatively modern,
..f-; 10,000 or 16,000 feet of sedimentary beds extended uninterruptedly
' \v^ r- from the South Park across the interval now occupied by the Sawatch
\i range, all of which, but insignificant remnants, have been swept away,
while a mass of tbe granite nucleus, of inconceivable dimensions, has
also been removed. The general elevation of the Sawatch range for
60 to 80 miles is 13,000 to 14,000 feet above the sea at this time, and it
is highly probable that hundreds and perhaps thousands of feet kave
been removed from the summit. I find it difficult to estimate the
extent of the erosion in this region, and can only speak of it in general
terms as almost incdnceivable to a finite mind.
From the nature of the interval or valley, the greater number of
streams fiow into the Arkansas from the main Sawatch range. They
are quite numerous from the Tennessee Pass to Canon City; a few come
in from the east side, but the drainage tends toward the east or south-
east, so that the streams that rise in the Park range and flow into the
Arkansas are comparatively few and of little importance. The charac-
ter of this drainage is well shown on the map accompanying this report.
In the last annual report I dwelt with considerable detail on the effects
of glacial action in this valley, and, in this report, I can only describe
them in general terms, hoping that the beautiful maps and illustrated
sketches by Mr. Holmes will render the story plain to the reader. As
an illustration of the effects of glacial action in this valley, Lake Creek
might be taken as an example. This stream rises in several branches at
the very crest of the divide, forming vast amphitheaters. The signs of
past glacial action are not very evident about the sources of their side-
branches, and they do not reach higher than 12,000 or 12,500 feet. Tbe
summits of the high mountains are often covered with debris of broken
rocks, apparently not much worn. In some places the tops of the mountains,
like Mount Lincoln for example, are, with the exception of the extreme
summit, covered with a thick covering of earth, filled with rocks more
or less worn. The most conspicuous signs of glacial action are seen
along the sides of the gorges lower down tbe streams. In the valley of
Lake Creek, the sides of tbe gorge are worn smoothly for an elevation
of at least 12,000 feet or above timber-line, and from 1,000 to 1,500 fleet
above the bed of the creek. In many places the sides of the gorge or
* canon are worn so smooth that the surface has the appearance of
enamel, and a thin crust usually peels off, which I have hitherto denom-
inated a " glacial crust." About four miles above the Upper Twin Lake
on the north side of the ciinon there is a round mass of granite
projecting from the side 300 feet or more, and 1,000 feet high, with
1
my
tt.
^x
.v^
/
•.
F/
v^f
./^^
'■V.
w>
■■'\
f '
^ V
-w/
:;x.v
V.
'-^^
5S^
5 AS VALLEY
1.
I
a, Oy, a, An
LoyFlatcuA
tlie Up]
I
M
GLACIAL ACTION — ^MORAINES.
49
roewhat the appearance of a bastion which has been worn qaite
ootb. Id the sides of it are depressions like pot-holes, evidently
vom oat by the attrition of loose rocks against the sides as the water
flowed andenieath the glacier. There are also points where vast masses
of granite have been removed from the sides of the mountain at a great
height, giving to the monntainside the appearance of an ancient quarry.
For a distance of abont eight miles the bottom of the valley will av-
erage one-fourth of a mile in width, with here and there huge masses of
granite projecting above the general level, showing very clearly that the
entire valley has been carved out of the solid granitic mass. The loose
iBorainal deposits are not conspipuons until we reach a point abont two
miles above the Upper Twin Lake, where the valley expands out to at>out
a mile to one and a half miles in width. Here a low swampy bottom
commences, which was once, undoubtedly, a portion of the lake. On
her side are ridges of the glacial deposits ; these increase in size and
ix>rtance as we descend to the junction of the creek with the Arkan-
On the south side of the lower lake a ridge extends from the
■ountains down to the Arkansas Eiver, perhaps 1,000 feet high, just
SDQtli of the upper end of the lake, and gradually sloping down 100 or
ISO feet in height above the bed of the river. This is a true morainal
fidge, and was doubtless formed by the crowding out on either side of the
Isoie materMs as the great glacial mass moved down the valley of Lake
Cieek. This morainal deposit undoubtedly laps on to the mountain-side
ID that the nucleus of the upper portion of the ridges is granitic. The
^ft deposits are not generally more than 500 to 800 feet in thickness,
and usually much less. The granite crops out in numerous places on
tte sides of the ridge, showing most clearly that the greater portion of
ils nucleus is granitic ; it also shows that the valley, with the surround-
kg terraced hills, has been worn down by erosion from an elevation
« great perhaps as the loftiest portion of the main range. The north
aide of Ijake Creek is a very irregular ridge, full of depressions, .while
m the west side of these ridges are extensive accumulations of rocks
vore or less worn, showing the direction of the moving force. Besides
fke vast lateral moraines in the valleys of the streams, there are a great
nmber of what may be called terminal moraines, or detached ridges
tUt tend in various directions. Sometimes they extend a portion of the
iktSLUCB aeross the valley at right angles to the lateral moraines, or
ttey may diverge at any angle ; the great quantities of loose material
ittaohed to the glacier seems to have been dropped in quite irregular
-fN'ms as it moved down the valley. In one instance the granite crops
fot at the east end of the Lower Twin Lake, about the middle of the
valley, and under such circumstances that the inference is plain that
tke entire valley has been worn out of the solid mass of granite. One
•f the main objects of our description of the morainal deposits is to
show the extent of the erosion which has taken place in this region,
tod tbese outcroppings of granite are the remnants that are left as
iroofs of the magnitude of this work. From Mr. Derry's house, on the
lorthwest corner of Lower Twin Lake, we have perhaps as good a
|pnen»l view of this valley and its surroundings as we can find. As
Ve look to the sonth of west we see two I'ront i)eaks, which are
Aaped like cones, rising up to the height of 12,500 to 15,000 feet.
i little to the southeast is an unnamed cone, with a broader sum-
it, rising above timber-line. Although these points or peaks ap-
ir to to independent, yet they are really portions of spurs or
gea extending down from the main peak, which extends further
the west and forms a part of the crest of the range, to which we
4 H
It
50 GEOLOGICAL SURVEY OF THE TERRITORIES.
have given the name of La Plata, 14,302 feet above the sea. As
look in this direction, bare, brown, granite masses, rising above timbe
line, meet our eyes, with here and there a few patches of snowtobre
the monotony or contrast with tlie desolate somber hue of the grani
debris. Deep furrows extend down the sides of the mountains, the chait
nels for untold ages of ice, snow, and water, the agents which have bra*|
ken down these rocky masses and sculptured the forms which now
much excite our admiration. We see also the smoothly-worn sides
the mountain covered with a sort of enamel-like crust, as a mark of the
glacial power. On the sides of the peaks, at different elevations, are nu-
merous small green lakes, sometimes with a visible outlet and some-
times without, reservoirs of the melting snows. The pines are oftei
dead from the autumnal fires that have run through, adding to the deso-
lation of the scene ; these falling down in every direction render travel-
ing almost impossible. Sometimes no vegetation takes the place of the
pines after the fires have passed through them, but not unfreqnently
the quaking-asp poplar, with its bright green leaves in summer and yel-
low in autumn, grow very densely, contrasting most charmingly with
the somber green of the living pines, and the somber brown or gray of
the dead. Down in the valley, and closed in on either side by mount-
ains and the morainal ridges or hills, are the two beautiful lakes, which
are laid down on maps as Twin Lakes, the basins of which were no
doubt formed by glacial action. If the reader will examine the map
accompanying the report he will see more clearly than we can describe ia |
words the location of the beautiful lakes, the morainal ridges and mouu^ !
ains that hem them in : the contour lines are not intended to indicate
elevation, but are used to show the surface forms. As there are really but
two forms, granite and morainal drift, but one color is needed, and with
this we have endeavored to separate the surface covered with the
morainal deposit from the granite. The map will also show the eleva-
tion of the lakes abo^e the sea, 9,182 feet; also the elevation at the
junction of the Lake Fork and the Arkans;}s, 9,096 feet. The depths <k
the lakes are shown by actual soundings. The greatest depth of the
upper lake is 79 feet, and that of the lower 75 feet. It will be seeu
that the greatest depth of the lower lake is near the upper end. We
may thus see by the depth of these lake-basins, as well as their shape
and morainal deposits around them, that the force that produced them
all moved slowly down from the mountain-range, and that the lake-ba^iiis
are scooped out of the solid granite rocks. From the lower lake to the
Arkansas Biver the morainal deposits are very thick ; the surface u
covered with bowlders more or less, and of greater or less size, some
small, others from 20 to 50 feet in diameter. Hundreds of mouuds,
ridges, and curious depressions, of ^all shapes and sizes, impede the
traveler. The placer-mining has been very extensive here, and by thia
means we arrive at the true character of this glacial drift. It is com-
posed mostly of rounded bowlders, but mingled with it is a kind of light*
colored clay and sand. Thedecomposition of the feldspar has produced $
kind of clay, which sometimes gathers into localities forming a cousick^
erable thickness.
The description of the glacial action in the valley of this branch d[
the Arkansas will apply to the others, and presents a general view of th
detailed action in the entire valley. The history of this valley from th
beginning may be in some points obscure, but, as I have stated in
former report, I regard it as largely due to erosion. In the process c
elevation a fissure or fissures must have been formed, and in these tl
process of erosion commenced, continuing through a vast period of tiiii<
MATVEx.] MORAINAL DEPOSITS. 51
aod operatiug with greater or less effect at dififerent portions of that
period. So far as tbe drift-deposits are concerDed, which at the present
time seem to be the only material resting on the granite in the valley,
tbey are nudoabtedly of comparatively modern origin, not extending
back farther than the Pliocene, but the beginning of the erosion may
reach into the past as far as tbe Jarassic. We have now the evidence
that indicates that portions of these mountain-ranges were elevated
above tlie Jurassic seas, and we may suppose that the general outline
of the surface continues on the same plan up to the present time. If
this was true — and we have no reason to believe the contrary — the erosion
may have, and probably did commence far back in the past, and that
daring the Cretaceous and Tertiary periods the area occupied by the
Sawatch range was elevated above the waters ; it is more probable,
however, that these formations were deposited to a greater or less ex-
tent over this area, and that they have been entirely removed or ground
up with the present drift. From the source of the Arkansas at the
Tennessee Pass to the canon above Canon City, the distance is about
60 miles, supposing this to be mainly a valley of erosion, area worn
away would average about eight miles in width, the depth could not have
been less than one mile, so that an approximate estimate can be made of
the enormous amount of rock-material has been ground up in the excava-
tion of this valley. Up to the time of the great glacial period this eroded
material may have been swept out on to the plains to assist in forming the
vast Cretaceous and Tertiary beds which we find there at the present
da>. Geologists generally admit that about the close of the Tertiary
period, there was an era of intense cold, which they have agreed to call
the glacial epoch, and our remarks are based on that supposition.
We believe that at one period this entire valley, with all the side-valleys
or canons, was occupied with one vast glacier, diminishing and in-
creasing as the temperature was higher or lower, but gradually moving
down; that is, the main mass moving southward, and the side-branches
moving toward the central mass. As the sides of the mountains are
worn smoothly and exhibit signs of glacial action to the height of at
least 1,500 feet above the valley, we may arrive at an approximate
estimate of tbe thickness of tbe glacier. The fissures of the Arkansas
and its branches may not have been nearly as large at the commence-
ment of the glacial period as at the present time, and the great glacier
may have performed the work of erosion for ages, and gradually melt-
ing by a change of temperature to the mild climate of the present time,
left the numerous mounds, ridges, and other morainal deposits which
we find so extensive in this valley, and in many other portions of the
Bocky Mountain region. I have spoken of this great ice-mass as a
single glacier; there may have been a single one increasing and dimin-
ishing through ages with tbe changes of temperature at different seasons
or epochs, or there may have been an unlimited number of glaciers, but
the glacial phenomena as indicated by the present surface of that
oonntry shows a long and continuous period of action. I have before
stated that I regarded the valley as one great lake-basin, commencing
Bear the Tennessee Pass. The valley expands out somewhat for the
Arst ten miles, and gradually closes up below the town of Granite for
about four miles, when it opens out again into a broad, level, basin-like
ibrm. The bottoms of the main river, as well as the little branches,
expose the granite rocks in such a way that we cannot well avoid the
conclusion that tbey have been worn "down to their present position
from an elevation not much inferior to the Sawatch or Park ranges.
Above the Lake Creek on both sides of the Arkansas are well de-
52 GEOLOGICAL SURVEY OF THE TEEBITORIES.
fined terraces, which on the east side rise 600 feet above the river.
The coarser materials were evidently deposited in water, and are
arranged in strata and appear not to have been disturbed to any great
extent by changes of level. On the west side the terraces slope down
more gradually, and are cut from west to east by deep gorges, by
streams from the main range. The valley itself extending to an eleva-
tion of 400 to 600 feet on either side, is filled up with more or less coarse
drift-deposits. These vary much at different points, sometimes made
up of huge bowlders, inclosed in loose gravel, sand, or clay, and again
a rather fine deposit of sand, gravel, or clay, to all appearances having
l>een deposited in comparatively quiet waters. At any rate there were
at all times portions of the lake that were not subject to great currents
or any violent agitation. On the whole, however, the drift-materials
are very loose, showing that the movements of the water and ice were
from north to the southward. All over the surface are scattered in
vast quantities immense bowlders of granite, varying from a few feet to
50 feet in diameter. Below Granite, for four or five miles, the masses
of granite are remarkable for their number and size, which appear to
have been moved down Clear and Pine Greeks. Along the sides of
Clear and Pine Greeks are high ridges, or lateral moraines, which may
properly be compared to huge railway embankments, rising to a height
of 400 to 800 feet above the valleys of the streams. Below the month of
Pine Creek the valley soon expands, and the surface is covered with loose
bowlders, while the ridges and depressions are quite remarkable, and
give it almost an artificial appearance. These basin-like depressions
inclosed by the moraines are not unfrequently filled with water, form-
ing small lakes, often with no visible outlet. These little basins of water
occupy different elevations, from the bottom terrace near the river to
the point of junction of the drift on the mountain-sides, 800 to 1,200
feet above the riverbed. As we descend the river the bowlders dimin-
ish in size, are more rounded, and the deposits of fine materials increase
in thickness. Below the mouth of Chalk Greek the valley is covered
with a series of yellow-white marly beds, which are cut up into a
variety of singular forms, resembling the ^^ Bad Lands" and reaching
an aggregate thickness of 800 to 1,200 feet. These were observed by
me in 1869 and named the ^^Arkansas marls." Overlying these marls
there is considerable thickness of coarse drift which forms to a great
extent the terraces which are very marked for a distance of 30 miles.
We can see, therefore, that the greater part of the finer sediments were
transported to the lower or south end of the river-lake, and deposited
in comparatively quiet waters. While we ascend the Arkansas Valley
toward the Tennessee Pass, the proofs of great force from the combined
action of water and ice are shown on a grand scale. It seems, too, that
while there is a variety of deposits in this valley resting upon the granites,
their history is consecutive and attributable to one general cause, local
glacial action, so far as I have yet observed. I repeat the same statement
which I made years ago, that I have observed no proof of any wide ex-
tended drift-action like that of the New England States, but in the Rocky
Mountains the superficial deposits are all of local origin : and the source
is usually limited to the drainage of the streams in wtiich it is found.
For example, although, as I have stated, I believe that all the marls and
coarser deposits in the valley of the Upper Arkansas have the same
origin, however different in composition, the forces that produced them
are limited geographically to the drainage of the Upper Arkansas. I
could find no indications that any fragment of rock had been transported
even from so short a distance as beyond the drainage west of the Sa-
H
MATDBx.l MORAINAL DEPOSITS. 63
watch or east of the Park ranges. It is possible tbat a more detailed
stody of the superficial deposits of this valley would afford reasou
for a separation iuto different periods so that they might be classified,
bat my observations lead me to place them in one great period extend-
ing from the close of the Pliocene up to the present time. As is shown
by the map, the drift-deposits rest upon the granite directly, and no
sedimentary beds of any other age are found in the immediate valley,
and these deposits in the aggregate do not afford proof of any break in
time. Still mach new matter could be added to the history of their
deposition if an entire season could be devoted to their study..
CHAPTER V.
General VIEW op the geography and geology of the Elk Mountains. — ^Erupttvk
GRANITES.— BhYOLITES AND DYKES. — EROSION ON A GRAND SCALE. — LoCAL DKUTT-
DEPOSITS.
The Elk-Mountain group is one of the most remarkable ranges in our
western Territories, and, so far as my own explorations have extended,
is unique in form and structure. For this reasofi a small party was
organized in the summer of 1874 under my immediate direction, with
Mr. Holmes as assistant geologist, and Mr. Chittenden as topographer,
for the special study of this curious and most interesting group. The
numerous sections and maps which are given in this report form a por-
tion of the results of this specific study. Much attention was given to
this region the previous year, and the results printed in the annual
report for 1873. As our explorations are extended to the westward of
this range, we hope to be able to present a more complete geological as
well as topographical view of this region.
The Elk-Mountain group lies immediately west of the great Sawatch
range, which forms the water-divide of the continent. It occupies an
area of about 800 square miles, between meridians 106<^ 45^ and 107<=^ 15',
and parallels 39° 30' and 39o.
The Sawatch group is one of the loftiest and most symmetrical ranges
in the West. It extends from the Mountain of the Holy Gross to the north,
latitude 39° 28', longitude 106o 28', southward to the San Luis Valley, a
distance of over 80 miles. For this entire distance the range literally
bristles with lofty points, about ten of which rise above 14,000 feet, anil
many more are 13,000 feet above sea-level. The uniformity of this great
mountain-mass is a remarkable feature. Standing on some high peak
and glancing along its pointed summits from north to south there seems
to be comparatively little variation either in foroi or height. On either
side of the Sawatch range there are several somewhat lower parallel
ranges which are undoubtedly portions of an immense anticlinal, of
which the main granitic mass is the central nucleus. Between each of
the parallel portions of the anticlinal are valleys at intervals of greater
or less width. Immediately west of the granitic nucleus is the valley of
the Gunnison, and on the east, the valley of the Upper Arkansas, and
east and west of them are comparatively low granitic ranges capped
with sedimentary rocks. Both the metamorphic and sedimentary rocks
incline at various angles from the great central mass.
There are here represented two quite distinct types of mountain ele-
vation, though the forces have influenced each other's results to a greater
or less degree. The Sawatch or main range presents an example of a
long-continued, uniform movement upward, which, but for the inter-
vention of side-forces, would have produced a remarkably symmetrical
mountain-group with the main granitic core or central mass, and on
either side parallel valleys and ranges, each becoming lower and lower
until the ridges faded out in the plains. The sedimentary rocks would
have inclined at various angles east and west from either side, until
they became horizontal in the plains. On the east side of the main
54
Rkjfolile
"Crtt. Shale
•ShyolUe
W ft. Shale
JO A RhyoiiU
Shale .
A portion of the £!aat /ace of Gothic Mt. ehoteinff the retatiotu of
the Eniptive Rockt to the CretaceouB Shatee.
', fc *
4 -,
# «
'a^
HiraEc.l GEOLOGY OP THE ELK MOUNTAINS. 55
raDge, in the South Park range, the eruptive groups have thrown the
sedimentary beds into the utmost confusion, producing those remaj'kable
£ialts and irregularities which were shown in the annual report for
1873. On the west side, in the Elk Mountains, the confusion is still
greater, producing not only the most remarkable faults in all the western
conntry, bat literally overturning thousands of feet of strata. By exam-
ining the preliminary map of Colorado in this report, it will be seen that
the trend of the Sawatch range is very nearly north and south, and that
tbe principal peaks from the Mountain of the Holy Cross at the north to
Mount Ouray to the south lie along that line. The trend of the Elk group,
tbongh less regular, will be seen to be about northwest and south-
east This is a grand illustration of an eruptive range, and appears
also to be an example of a sudden violent or catastrophic action. The im-
mense faults, complete overturning of thousands of feet of strata, and the
great number of peaks, all composed of eruptive rocks, indicate, perhaps,
periodical and violent action in contradistinction to long-continued uniform
movements of the elevatory forces. The sections and maps which acconj-
paoy this rei)ort will doubtless enable the geologist to determine tbe cor-
rectness of our statements. The map will show by the colors the erup-
tive points, where the granite appears to have been thrust up, as it were,
through the vast overlying crust; sometimes a great thickness of
strata of various ages is carried up to the summits of the peaks, 13,000
or 14,000 feet in elevation above the sea. Again we find, but a few
jards away, the same group of strata in the bottom of the lowest val-
leys, indicating remarkable convulsive movements. Although the Elk
group may be regarded as an eruptive range, it will be seen by the map
aod section that the elevatory forces, whether convulsive or uniform
ami slow, acted along a well-defined axis, thus, as a range, forming a true
anticlinal.
We see, therefore, that the eruptive agents acted along a great fissure
Id the earth's crust as a line of greatest weakness, and that this line
lK)«se8sed a trend about northwest and southeast. But the peculiar nature
of tbe forces produced the wonderful chaos in the position of the sedi-
mentary beds, while the tendency of thesestrata is toincline from either side
oftbe axis. It is not uncommon to find thousandsof feet of strata which
have been carried up to the loftiest points of the axial ridge in nearly or •
quite a horizontal position. We may suppose that at one period the vast
sedimentaiy mass rested on a floor of pasty or semi-pasty granite; that
the forces in the interior were struggling to find vent, carried upward
the entire overlying mass of sedimentary strata, and that here and
there many thousands of feet in thickness along the axial line or ridge
van thrust up through tbe melted or serai-melted granite in such
masses as are shown on the map, at Italia, White liock. Snow Mass, Capi-
tolaiid Soprls Peaks. The map will show that this igneous granite does
not reveal itself except along this quite regular axial line. The areas
of granite are greatly enlarged by subsequent erosive action, while
from the axis numerous streams cut deep gorges, 1,500 to 3,000 feet in
<leptb, sometimes far into the underlying floor of igneous granite,
boring this period of revolution, and probably subsequently, there were
igreat numbers of dykes or orifices from which issued the rhyolites and
A^asalts. Gothic and Crested peaks are illustrations of the upthrust of
vast masses of rh^olite, and numerous other quite long dykes will be
noticed on the map.
Plate XIV represents a portion of the east face of Gothic Mountain,
^he central mass of which is rhyolite, with only the Cretaceous beds
lilted up around the base and sides. This is an excellent example of these
56 0£OLOGICAL SUHYEY OF THE TERRITOBIES.
remarkable npthiiists of iproeons material, Tertically through the over-
IjiDg sedimeutary beds. The Cretaceous strata of Nos. 3 and 4 extend
up OD the aides of the peak about 1,000 feet above the bed of East
River, with very little inclination, and between the strata of shale were
pressed out portions of the igneous material.
The illnstmtion, Plate XIV, is so clear that but little space need be
used in explanations. The shale all belongs to Cretaceous formation
No. 4. An examination of the map and plate of sections would indicate
that the aggregate force which elevated the Elk range acted vertically
with a tangential movement or shove, as it were, from the northeast toward
the southwest. There are many faults of remarkable character on the
northeast side of the axis, but no very marked examples of the inversion
of strata, but on the southwest side of the axis this feature is shown in
a. marked degree. Time will not permit us to work out in detail in this
report the wonderful complications in the strata, which have been pro-
dnced by the various elevating forces in this range. Much of it was
brought out in the various reports in the annual report of the survey
for 1873. Mr. Holmes will also introduce important details into his
report. I shall, therefore, at this time, confine myself to a general view
of the geology of this range, which, with the l>eautiful and remarkably
clear illustrations, will be sufficient for the information of the geologist.
The axis of the Elk range can be easily traced on the map, and the
axial section will show the immense masses of strata that were carried
high up to the very summits of the range.
At the southeast corner of the map it will be observed there is a con-
siderable area designated as metamorphic granite. This forms a part
of the Sawatch Mountains, and may serve to show the relations of that
range. To the west of it there are narrow belts, marked as Silurian
and Carboniferous. These represent masses of strata that were origi-
nally lifted up by the Sawatch range and incline toward the west On
the completed geological map of Colorado, the connection of thei«
fragmentary masses of sedimentary strata about the summits of the high
granite mountains will be made clear. We shall hereafter attempt to
show by a series of sections, not only that the Triassic, Jurassic, and
Cretaceous groups originally existed here in full force, but that they
probably extended across the area now occupied by the Sawatch range
and were united with the sedimentary beds of the South Park range.
The northeastern slope of the Elk group slopes down into the valley
of the Roaring Fork, an important branch of Grand Biver. Here we
find a large area of the various divisions of the Cretaceous group. The
Dakota group rests upon the Jurassic, but is not exposed to any great
extent, except in.the canons or gorges of the streams. So far, therefore,
as a map is concerned, it cannot be represented except by a very nar-
row band, but above it there is from 1,000 to 1,500 feet of the remaining
portions of the group, Nos. 2, 3, 4, and 5, but not as well defined even
as on the eastern side of the Colorado or Front range. The greater
portion is composed of black shaly clays with thick beds of sandstones
appearing in different positions. A few Cretaceous fossils occur, of well-
known and common genera, as Amfnonites^ BaculiteSj and Inoceramus.
Very few of the smaller forms were observed. This singular Cretan
ceous area seems now to form a sort of basin with the Jurassic and
Triassic, or Bed Beds all around it. Its peculiar form will be noticed
on the map. The Cretaceous beds occupy very varied positions,
sometimes high up on the mountain-sides nearly to the summits,
and then filling up the lower valleys. The faults are without numr
beTi for in the process of elevation the strata seem to have been
N^
■ATMH.) GEOLOGY OF THE ELK MOUNTAINS. 67
Iwoken in every direction. The aggregate inclination, however, is
always to the northeast. This great mass of Oretaceoas beds were
ioflaenced by the operations of two quite distinct elevatory forces which
]irobably acted synchronously, so far as forces so different could act.
To the eastward the long ridges of the Triassic and Carboniferous Bed
Beds extend down to the west from the axis of the Sawatch range, cut
into deep canons, the waters of which flow into the Grand Biver.
These Red Beds were elevated by the Sawatch range, while the Bearing
Pork flows through a sort of anticlinal valley between the axis of the
£lk and the Sawatch Mountains. These Cretaceous beds form a sort of
u island or basin between these great axes, and therefore lie in the syn-
clinal. It is by means of the more modem beds, as the Cretaceous group,
that the anticlinal character of the mountain range is more clearly seen.
The Triassic and the Carboniferous beds extend over the axis of the
range, while the granite nucleus makes its appearance only in limited
areas, as at Sopris, Capitol, Snow Mass, and White Bock i)eaks. Be-
tween Capitol and Sopris i>eak6 there is a long distance where the Bed
fieds form the axial ridge entirely, and seem to hold for the most part
a horizontal position. On the map the Bed Beds or Triassic and the
Carboniferous groups are thrown together, from the fact that we found
Tery great difficulty in separating them. Not only is there no apparent
break in the sequence of the strata, but they are so mingled together
in the uplifts and overtumings that it would have required more de-
tailed study of the range to separate them entirely than we were able
to givf) at that time. Co-extensive with the narrow belt of the Dakota
^ap, IS a light band which represents the Jurassic group. Neither of
these formations is ever exposed over large areas, usually only in out-
cropping edges along the margins of the mountain, or in the sides of the
canons. The Silurian group, so far as it is known in this region, always
rests directly on the granites, whether igneous or metamorphic, and is,
therefore, confined mostly to an outcropping belt around the granite
areas. On the west and southwest sides of the axis the Cretaceous
groap appears again, extending far beyond the limits of the map. Its
relatioDS to the axis are such as to show plainly that, like the older
fermations, it formerly extended in an unbroken mass across the area
of the Elk range. There can be no doubt of the original continuity of
the entire mass of the sedimentary strata. North and west of Sopris
Peak the country slopes ofl: toward the Colorado Biver, and the sur-
fm is gashed deeply with the gorges of the streams which cut through
the Cretaceous beds, oftentimes into the older groups. The Cretaceous
itrata, however, predominate.
In the annual report for 1873, the tremendous effects of erosion, as
shown on the west side of the Elk Mountains, were described in detail.
These effects are displayed even on fk still grander scale on the east side
of the range. The gorges or cafions cut by Castle and Maroon Creeks
and their branches, are probably without a parallel for ruggeduess,
depth, and picturesque beauty in any portion of the West The great
Tariety of colors of the rocks, the remarkable and unique forms of the
peaks,' and the extreme ruggeduess, all conspire to impress the beholder
with wonder. The illustration, given in the northeast corner of the
Mp, of Castle group is a type of the scenery at the heads of these
streams. We here see from 3,000 to 5,000 feet of stratified rocks lifted
op vertically so that the beds are horizontal, or nearly so, presenting to
the eye, by the eroded forms, a wilderness of pyramidal cones whose
sammits rise to a height of 13,000 and 14,000 feet. The sides of the
saiions are vertical or nearly so, displaying a continuous section of the
58 GEOLOGICAL SURVEY OF THE TERBITOBIES.
Strata 2,500 to 3,000 feet, composed of alternate beds of sandstones and
conglomerates with thin layers of clay or shale. . These sandstones vary
very much in structure in the same layer, from a fine-grained sandstone
or quartzite to a rather coarse conglomerate. These changes may occur
in different portions of the same layer or at different positions in the
same group of strata. The lower portion of the canon is composed of
rather compact sandstones, but toward the summit the rocks become a
brick-red and are formed of rather loose sandy material. All the rocks
vary in color from a dark dull purple to a brick-red, depending much
on the influence of heat. There is a considerable degree of change in
these rocks from heat, but only in a few cases amounting to complete
metamorphism. These massive walls and pyramids are often inter-
sected with dikes which have filled either vertical fissures or not un-
frequently have been thrust between strata, forming local beds of
rhyolite, sometimes of great thickness. The dividing ridge forms a
curious zigzag line, often so narrow as to be almost impassable to one
on foot.
Enormous amphitheaters have been slowly carved out of the dividing
ridge at the head of each little branch. Without speculating upon the
character of the forces which were at work here in the far past, whether
they were far more intense in their action than at present, we may infer
that at this time they operate exceedingly slow. Portions of the divid-
ing wall are falling all the time, from the influence of frost or water, and
in many instances the amphitheaters extending back over the true di-
vide, sometimes even breaking through the axial ridge. Usually a vast
accumulation of debris may be found damming up the gorge at various
distances from the immediate head of the amphitheater, thus giv-
ing origin to a small lake, the waters of which gradually soak
through the debris^ and, coming out on the lower side, gather into a
small stream. It seems hardly possible that at the present time there
are any agents in existence that could have transported this debris
down the gorge. It must have required a considerable quantity of water,
with large masses of snow or ice, for the debris is often composed of
large masses of rock that could only have been moved by floating ice.
In the valley of Roaring Fork, the morainal deposits are remarkable
for their thickness. The surface is covered with huge bowlders, some
angular and others partially rounded. The terraces are very conspicu-
ous, rising, in some instances, to 1,000 feet or more above the bed of the
stream and strewed over with huge bowlders. None of the stray ma-
terials in any of these valleys or gorges seem to have been transported
a very great distance, and never, under any circumstances, is there any
drift or glacial deposits from a neighboring drainage; in other words,
the loose material does not pass from one independent valley to another.
So it is all over the Rocky Mountain region so far as I have observed.
All the drift or Post-pliocene deposits are local.
I regret that, for want of time, this meager account of so important
a range of mountains must be closed. In the final report, in quarto^
which will accompany the atlas of maps, we hope to present a more
caretul review of each range of mountains, with their relations to eacli
other.
In this report I have attempted to number the plates In consecutive
order, but the sheets of sections and maps could not be so numbered,
but will probably be clearly understood.
CHAPTER VI.
yj
EEPOET ON THE GEOLOGY OF THE 3SORTHWESTERN POE-
TION OF THE ELK KANGE.
By W. H. Holmes.
Dear Sie : In accordance with instructions received from you, I con-
tinued the geologic examination of the northwest portion of the Elk
MonntainSy and beg leave to present the following report:
When it was found that, on account of the sickness of Mr. Shanks,
assistant topographer, the main party could not advance beyond Capi-
tol Greek, a small party, consisting of Mr. George B. Chittenden,
topographer, myself, and one packer, was detailed to continue the survey
around to the northwest.
It was arranged that we should carry with us provisions for fifteen
days, and that a supply-party should meet us on the western side of the
laDge, near the sources of East Eiver, if the main party should not be
able to reach that point in time.
On the 29th day of August, we left the main camp and moved down
tbe valley of Eoaring Fork. A well-marked Indian trail led us through
a low, synclinal depression, which is separated from the channel occu-
l>ied by the river, by a long, narrow ridge or hog-back. The depression
is occupied by the Lower Cretaceous shales, and the sandstones of the
Dakota group form the crest of the ridge.
We soon crossed a low divide and were upon the southern branch of
Sopris Creek. This stream heads near the summit of the Elk range,
midway between Capitol and Sopris peaks, and on reaching the deepest
prt of the dexiressiou, turns abruptly to the northwest and cuts ob-
liqaely down through the ridge of Cretaceous, Jurassic, and Triassic rocks.
Tbe main Sopris Creek is formed in the snow-filled amphitheaters
about the eastern faces of Sopris peak and descends to the valley with
great rapidity, falling G,000 feet in less than eight miles. It cuts its
wayout from the granite to the Cretaceous rocks and then descends
witb tbe dip of the beds, flowing for some time upon the hard floor of the
Dakota sandstones. The bed of the ereek is everywhere very shallow,
and I was unable to determine whether any rocks lower than the Ju-
rassic were exposed or not. Dr. Peale, who climbed Sopris peak from
this side in 1873, states that there is but little exposure of the sedimen-
tary rocks along the north and northeast faces of the mountain, on ac-
count of the great quantities of debris and morainal drift.
TIIE KOARINa FORK SYNCLINAL.
Before passing on to the description of Eock Creek and the western
slope, I wish to take a hasty review of the general geology of the valley
of Roaring Fork, and give, if possible, a connected idea of its structure.
I'bis valley is throughout, so far as examined, in the trough of a syn-
<}liiial fold, and its entire conformation, the course and form of the main
valley as well as of all its tributaries, is undoubtedly the result of this
59
60 GEOLOGICAL SURVEY OF THE TEREITORIEg.
geologic condition. The depression is by no means uniform, and the
movements of the stream-bed are quite eccentric, making altogether a
very interesting study.
From the mouth of Maroon Creek to the mouth of Sopris Creek, a
distance of some twelve miles, there is a pretty well marked fault, not
following the line of greatest depression, but occurring along the easteni
slope from one-fourth to three-fourths of a mile from the axis of the
fold. We thus have a fracture parallel with a fold, and the two lines
seem to contend for the privilege of accommodating the stream-bed.
Above Maroon Creek (see map and sections) the river flows in the syn-
clinal ; near the mouth of the same creek^ it is in the fault. Below this
it cuts through the beds again and follows the synclinal for a number ^^
miles. Still lower it turns again to the right, into the fault, and follow^
it all along the eastern base of the isolated ridge mentioned at the out-
set. Leaving this again below the month of Sopris Creek, it continues
iu the fold, while the fault probably dies away. The dislocation, if any,
of the beds, as exposed on opposite sides of the stream, is so slight that
it seems quite impossible to determine this point. The downthrow is
generally on the west, and does not amount in jany case to more than
3,000 feet. In two localities along the faalt, there have been outflows
of lava. These were observed by Dr. Peale, in 1873, and are located,
the lower one, opposite the mouth of Sopris Creek, where it cat)salarge
rounded bntte, (see general map.) The other is on the same side of the
river, some five miles farther up. The lava appears to be basaltic, and
has quantities of cinder and ashes associated with it It caps an Im-
portant butte near the river-bank, forms an escarpment some 100 feet in
height, and covers an area of scarcely more than half a square mile.
Section C of the large sheet cuts this butte, and shows at the same
time a most remarkable displacement, the edges of the strata on botli
sides of the fault being turned abruptly up, and therefore dipping
from the plane of the fault, both toward the upthrow and the down-
throw. The beds on the west side are depressed so that the Lower
Cretaceous rocks seem to face the Upper Carboniferous of the east side.
The upturned edges were apparently leveled off before the flow of
lava took place. At the mouth of Maroon Creek the depression of
the west side has been much greater, and the edges of the beds have
been dragged upward and, apparently by a lateral movement, forced
past the vertical. Thus is formed the little butte of Cretaceous and
Jurassic rocks between Maroon Creek and Bearing Fork, at the junc-
tion described by Dr. Peale, (Report for 1873, page 263.) Shortly above
this the fault becomes a fold and so continues up the valley of Castle
Creek.
The sections of the accompanying plate, Fig. 1, cut ten of the most in-
teresting points along the line of disturbance, and is intended to give a
connected idea of the folding and dislocations. The sections are so placed
as to give fhe impression that perspective is taken into account and that
the point of view is somewhere on the lower course of Bearing Fork. It
will be observed, by reference to these, that the southern extension of
the synclinal follows the valley of Castle Creek, and that the upper
course of Boaring Fork proper is in the granite to the east. A still
more extended examination to the southward and beyond the sources of
Castle Creek, seems to warrant the conclusion that the portions of Silu-
rian (t) quartzite noticed on the east face of station 3 and along the
summit of the Italian group beyond, indicate a continuation of the same
fold or alt least of the same movements that produced the fold. That
this is the case, and, therefore, that the entire geologic phenomena of
F' '■' Jtalien ML
"**
• • » -^
^
l'» 'I
«/
I *, \*s'
^ ..
) » >'.•.»'''• ';,
^x X ' ^.; v-cX'.^'.
8
'.y» •
» V •
f %
. 9
X ' >"^. , •• '
•p-
10
^^
FIG. 1.
Tm Sections across the /Synclinal Valley of the Roamng Torkj
partially in perspective.
V
**•*/>"
/.
0r*
JLibrary. j
Of
(•.;ft>Tt.'i»
nouas.^ 80PRIS PEAK. 61
this region are connected, and, generally speaking, not tbe result of
complicated causes, may be pretty conclusively shown.
It mast be noticed, in the first place, that on the east side tbe sedi-
mentary strata lie up against the granite of the Sa watch range, and that
on the west they have been carried high up on the arch of the Elk
3Iountain8, leaving the synclinal depression between the ranges. In the
second place, that the axes of the two ranges are not parHllel ; that they
approach each other toward the south and separate toward the north,
. giving au included angle of some 3(P. In the vicinity of Italian peak
the granites of the two ranges are in contact, or nearly so, as seen at a
in section 2. On station 3, a few miles farther north, a fragment of the
Paleozoic rock is caught up and held, as in a vice, between the masses
of eruptive and metamorphic granite, &, section 3. North of this, down
the valley of Castle Greek, tbe sedimentary area widens rapidly. The
edges facing the Gasile group are bent up at a sharp angle, but as the
fold widens it also fattens, so that 30 miles north of Italian Mount-
ain, near the line of section 10, the belt of strata is 25 miles wide and
has nowhere a dip greater than 10^ or 12^.
In tbe plate I have indicated the two granites by different symbols,
the metamorphic by short broken lines and the Elk Mountain granite
by dots. The points of contact, as shown at a, 5, c, &e., are, of course,
only given to indicate a probable contact line. That such a separation
really exists, however, is evident from the fact that when observed in
close contact, near Italian Mountain, they are totally distinct in appear-
ance and in reality. In all itB general features, the geology of the val-
ley of Hoaring Fork and of the eastern slope of the Elk Mountains,
6eems simple enough, and I shall hasten on to the north and west.
6E0L06T OP SOPEIS PEAK AND VICINITT.
Having ascended Bopris Creek for some five or six miles, we turned
abraptly to the right and crossed the low divide that connects Sopris
peak with an outlying triangular spur, and descended by a deep gulch
into the valley of Rock Greek. We reached this creek at tbe point
where the upturned edges of Gretaceous No. 1 (Dakota group) cross,
and found that our descent had been almost with the strike of tbe beds,
^^40^ w. This is on the west slope of the Eoaring Fork synclinal, and
the dip is therefore to the east. The creek passes out into the Gretaceous
shales and reaches the river some eight or nine miles below. The
crossing of No. 1 here marks the foot of the caiion of Hock Greek.
Beneath No. 1, on the south side, a very beautiful section of the
Jurassic is ex]K)sed. Near the summit of the blufi", about 200 feet of the
^wer Gretaceous measures are exposed, consisting principally of com-
pact yellowish sandstones. Some thin beds of shale are iuterstratified
^ith the sandstones, and near the base there is an irregular stratum of
iQoderately coarse conglomerate. The Jurassic section, beginning at
tbe top, is as follows :
'^ feet shales, containing seams of greenish and purplish guartzite. The
Bhales weather like fire-clay.
^»feet thinly laminated, fine-grained, flinty quartzite.
10 feet yellowish quartzite.
W feet shales and calcareous sandstones.
^ feet sandstones and sand shales.
^ feet yellowish sandstone with layers of gypsum.
■^ ahales and red sandstones of indefinite thickness.
From the trail, near tbe creek-bed, a yery fine view of this cliff is
62 GEOLOGICAL SUEVEY OP THE TERRITORIES.
obtained. Weathered into the nsaal forms produced by alternate bard
and soft beds, it begins at the top, by an escarpment of the yellow
sandstones of No. 1, passing down into purplish and greenish gr^ySj
broken by darker lines of outcrop, each of which gives a tinge of its
own color to the already highly-tinted slide, and still farther down the
wide band of rich yellow transforms all to its own hue, and the whole
sweeps down like a gorgeous curtain over the bright red cliffs of
the Triassic (?). The closest search developed no trace of fossils, and
it is of course impossible to define the limits of the several periods.
The lithologic gradation here, from the Jurassic down through the
" Ked Beds ^ into the well-established Carboniferous is most perfect, and
Ihe entire absence of fossil-remains leaves us without a clue.
In passing up Rock Creels we descend through the strata and on either
hand find the caSon-walls composed of the red and maroon Carbonif-
erous series. On the left they support the Sopris mass, which stands
some miles back, and on the right rise into a cluster of rugged hills,
above and beyond which are the lines of Cretaceous outcrop, apparently
dipping to the westward. In the bottom of the canon the maroon beds
seem, very oddly, to dip toward the Sopris uplift as if not affected by it,
but by some movement farther to the west, but they are doubtless folded
abruptly up against the northwest face of that mountain. Close under
the west walls of Sopris the creek forks. At this point the granite
appears, and may be seen, from far below, rising in rugged walls and
abrupt spurs. The two branches seem to emerge from the base of
these as immense springs, but by a closer approach we could detect the
canons through which they flow. They are cut like great gashes through
the granite, having between them a high promontory.
On the 30th of August we ascended this promontory, and found it to
be a very excellent point of observation (station 22). The peak lies to
the east, rising very abruptly from the creek and presenting an aston-
ishing mountain-slope. The creek-bed is 6,000 feet above the sea, and
tbe peak springs to the height of 12,800 feet in one precipitous, un-
broken slope, a rise of 6,800 feet in one and a half miles. With the
exception of this western tongue, the granite mass seems to be a per-
fect cone that has had its apex pushed through the sedimentary strata,
lifting them up abruptly all around, but in no case affecting them out-
side of a radius of three or four miles. Indeed, if the erosion had been
more equal on all sides the exposed granite area must have been nearly
circular, but the great erosion of Rock Creek cutting so deeply into the
mountainside, has developed an area something like that shown in
Fig. 2.
This elevated area forms the extreme northwest end of the Elk range,
and is connected with the Capitol and Snow Mass groups, which lie
about ten miles southeast, by a high, red ridge, the crest of an arch in
the Carboniferous rocks, which here connect completely across the
range. The more recent strata have been broken down and carried
away, so that their outcropping edges are ranged low down along the
flanks of the mountains, on the east side trending toward the north-
west, making almost a tangent with the Sopris granites, crossing llock
Creek at the point where we entered the valley, and swinging around
to the north indefinitely, but, very probably connecting, in the low
country, with the corresponding series of the west side.
The east branch of Hock Creek, which I have called Avalanche
Creek, heads in the northern and western faces of the Snow Mass
group, and has cut its way in a most remarkable manner down through
the side of the red arch, almost parallel with its crest, striking Sopris
^C \ :
GrarateLSSol Silurisin(>l llllillli CailHmifmniB !
Fig.Z.
Fig. 3.
Section across ttie Sopris upbft.
x . f • ■-■ - ■^' ^, \
• /« ■ . • }
\ '^'^■"•ro-
\fA
'J^ A
J
^
Il
111
flfl'
IJI-
B 'J
II
II
Boua»] VALLEY OF KOCK CREEK. 63
between onr station and the main summit, and joining the main stream
below. In the npper course, therefore, it is in granite, in the middle
part, in Paleozoic rocks, afterward in granite, and finally again in the
stratified rocks, cutting its way, after joining the main stream, from the
8iluriaQ out into the Upper Cretaceous. Eock Creek proper, the
soorces of which were explored last year, can be traced far to thesonth-
wartl, as it comes down through a deep valley. This valley widens as
it approaches our station, but on reaching the belt of granite, suddenly
closes into a deep and precipitous canon. This is immediately under
us, to the west, and a stone dislodged plunges down over the crags
to the creek-bed, 1,500 feet below. This canon is hardly more than
half a mile in length (the width of the granite arm) and opens below
into the great triangular valley about the creek junction.
The sketch on the opposite page, Figure 4, will aid in making clear the
geology north of our station, and about Sopris. As seen in the drawing,
t here is considerable irregularity in the disposition of strata. The isolated
fragment of Paleozoic beds between Sopris and Eock Creek evinces a
considerable amount of lateral crushing as indicated by a series of
abrupt and angular concentric folds or wrinkles. Along the line of the
creek-bed there has probably been a slight dislocation or fault as indi-
csated by the want of harmony between the strata at e!' on the east side,
and those at t"' on the western. There are also traces of a considera-
ble degree of metamorphism, shown by the change of color near the
granite contact, as well as by the thinningout of the entire series, such
a8 would occur in a number of sheets of iron heated and partially welded
together at the edges under the irregular blows of a hammer. It has
been saggested that the existence of a shoreline about the granitic area
has, during Paleozoic times, produced this thinning-out, and especially
since, on the eastern face of the mountain, the more modern deposits
seem to jut up against or almost against the granite, but it should be
observed that in every locality where this peculiar granite appears, there
are unmistakable evidences of abrupt and violent movements, inde-
pendent of its relations to the sedimentary strata. It acts in all cases
as a foreign element, plastic and aggressive, intruding itself upon a
region heretofore undisturbed, and producing disturbances of the most
marked and unusual kind. In this case, however, there is less evidence
of violence than in any of the cases farther south, but in lithologic char-
acter and methods of upheaval it is the same.
GEOLOGY OF THE DISTEICT DRAINED BY KOCK CREEK.
We bad resolved to follow the course of the western or main branch
of Rock Creek. In the canon there was an old trail leading over the
rocks, and we passed through, without difficulty, into the open valley
above. Here were some beautiful meadows in which we discovered a
group of hot springs. In a number of places, steam could be seen rising
from 'the grass and reeds, and on approaching we encountered a number
of slimy pools, from which considerable streams of hot water were flow-
ing. In all there were more than a dozen active springs, in most cases
impregnated with sulphur, and ranging, in temperature, from 30^ to
1040 F.
On the 29th a rain-storm had set in, and everything was now wet,
thoroughly saturated. Muddy torrents poured down the upper slopes
and dashed over the cliffs into the valley. Avalanches of wet earth,
carrying many rocks and trees, formed near the summits and came roar-
ing down, discharging their great masses of i&}ri» into the river, and
G4 GEOLOGICAL SURVEY OF THE TERRITORIES.
tearing oat snch gorges in the alluvial bottoms as to make travel almoat
impossible. The coDtiuuation of this sliding process from jear to year
keeps large portions of the monntain-sides swept clear of all movable
material, leaving only the bare rock. Ail along these deep valleys such
avaianche-pathways may be noticed.
The vegetable growth is qaite profase in this region. Dense groves
of aspens occupy the more fertile spots, pines and cedars cling to the
rocky slopes, while scrub-oaks and a great variety of smaller bashes
abound. There is but little room for agriculture or grazing.
At the upper end of the cafion the granite disappears and the yellow
quartzites descend into the valley and also disappear, dipping *30o S.
The Carboniferous maroon beds follow, but soon assume a horizontal
position^ so that there is nothing else exposed in the walls, for a distance
of Hve or six miles. Then, by an abrupt monoclinal tbld, the whole
series pitches into the valley, leaving nothing exposed but the massive
sandstones of the CTpper Cretaceous. These beds in turn assume a hori-
zontal position, forming shelved slopes to the height of 1,200 to 1,500
feet on either side of the creek. The creek cuts obliquely through this
fold, and the section exposed consists of the Upper Carboniferous,
Jurassic, and Lower Cretaceous strata. On the left hand the hard layers
of the Dakota group, standing almost on edge, form a high ridge that
extends to the southward up the western slope of the Snow Mass group.
On the opposite side, the trend of the same beds is to the northwest,
passing up the face of a high mountainous ridge which culminates in
Ganuett's station 26, ten miles west of Sopris. Sectioa C of the large
sheets cuts this fold near the creek-crossing, and also gives a transverse
section of the great red arch which lies between Sopris and Capitol peaks.
The facilities for measuring the strata in this locality are very poor.
The yellow quartzites, supposed to belong to the Silurian age, do not
measure more than 500 feet, while the Carboniferous series will hardly
fall short of 4,500. The Triassic (f ), Jurassic, and Cretaceous beds will
add about 5,500 more, so that the exposed strata will include a thickness
of some 10,000 feet.
Ever since entering the valley a handsome group of mountains had
been in sight, apparently standing in the valley-course, and quite cut-
ting off the view. From the crossing of the monoclinal fold, the first of
these mountains appeared three or four miles farther up, standing on
the west side of the valley, and rising abruptly from the creek. We
determined to climb this in order to get good views of the Elk Mount-
ains, which lie mostly to the east, and of the unknown area to the west.
In the first place, we ascended the steep Cretaceous slope to the right,
at its lowest point, and found ourselves on a level with the undulating
country to the west. Gannett's station 26, was on our right, some ten
miles to the north, and the mountain which we desired to climb on the
left, three miles away, and rising nearly three thousand feet above us.
Following the summit, or back of the ridge which leads up toward it, I
observed that the Cretaceous strata were rising with the slope, flud at
the base ot the steeper face were turned sharply up against it at an
angle of 45^. In crossing these upturned edges, I observed that they
comprised no great thickness ; that the bulk of the sedimentary beds
seemed not to change from their horizontal position, and that this up-
turned portion had been separated from the rest and forced upward by
a wedge-like mass of intrusive rock which belonged to the central mass
of the group. (See Figure 5.) These strata seem to belong to the Cre-
taceous Coal Measures, as there were outcrops of coal and carbonaceous
shale. The horizon would hardly be less than 3,000 feet above No. 1.
'A»ftJ»
J SNOW MASS GBOUP. . 65
The rock of the peak proved to be an exceedingly fine and handsome
rbjolite, grayish in color, and containing many large crystals of white
feldspar.
Station 23 was made near the highest point. This proved, as I had
expected, to be the extreme northern summit of the large groap of
moantains that lies to the west of the Elk Mountains proper, and may
for convenience be called the West Elk group. It is hardly inferior to
(be main range in area, and is separated from it by the valleys of Bock
Creek and East Biver. Clusters of handsome, moderately high summits
eonld be se«n far to the southward, and as far toward t^e east as Treas-
my or Lookout Mountains. The general outlines and the manner of
weathering indicate that they are all of trachyte or rhyolite.
To the westward the country is low, and slopes off toward the Gun-
Bison Biver on the left, and the Grand on the right. There are no
striking geographical features, and the whole visible area is doubtless
of Cretaceous age, the exposed rock being mostly of the Upper Creta-
oeoas group, which comprises perhaps 2,500 feet in thickness of sand-
stones, conglomerates and shales, with an undetermined number of coal-
seams.
As mentioned before, the main body of the stratified rocks abtjut this
station are not disturbed, so that the exposures all along the eastern
base, beneath, the body of trachyte, are horizontal, and so continue far
op Bock Greek. This creek heads in a picturesque group of nioun-
taios far away to the east, cuts its way down through a number of deep
eanoDs, and striking the base of this mountain turns abruptly to the
north. Prom this point we get our first view of the western faces of
the Elk Mountains, and are impressed more deeply than ever with
their beauty and grandeur. The lower slopes are underlaid by Cretar
taceous strata and densely covered by a growth of gray and purple
onderbrnsh. Above this, groves of aspens and clusters of dark blue
pines relieve the glowing reds and purples of the Gaiboniferous rocks.
Still higher, and in delightful contrast to these ardent colors, are the
sammita of gray granite, whose polished and ornate faces constantly
remind us of the form in some gothic cathedral. The culminating sum-
mits belong to the Snow Mass group, and are so thoroughly hemmed in
by seriated crests, and deep zigzagging ridges, that they seem to chal-
^ge approach. In a few days we hope to penetrate the obscure
^slleys that bead in this group, and from some of its higher peaks make
ft more detailed study of its forms and structure.
We found theasceutof Bock Greek besetwithdifQculties,and only suc-
ceeded in advancing at all by climbing the eastern wall of the canon and
lemaiaingon a fiat, shelf-like area, formed by the horizontal Cretaceous
ftrata. In the middle of the afternoon of September 1st, we descended
iBto the bed of a small tributary of Bock Greek, not far below the base
^ Treasury Mountain. In passing down the face of the upper ledge 1
<^bierved th^t the rock was of rhyolite, and not sandstone, as I had
supposed. This proved to be only a capping, and is doubtless a rem-
Bant, separated from the mass west of the creek by erosion, since both
v^Us of the valley, up to corresponding horizons, are of Gretaceous
The creek into which we had descended seemed to issue from the very
^terof the Snow Mass group, and finding a pretty distinct game-trail
^e tamed to the left and tbliowed it up the valley. On our left hand a
f^ bluff rose to the height of some 1,500 feet. The strata exposed in
1*8 face were probably of the Upper Gretaceous group, and consisted of
^dstones and shales, the former predominating above and the latter
5 H
66 GEOIiOGICAL SURVEY OF THE TERRITORIES.
below, so that there was a gradation from solid sandstones at the top
to homogeneous shales at the base. The section includes the groap of
strata sometimes called the ^^ transition group" by Dr. Haydeu. The
horizon is probably that of the upper part of No. 6, Cretaceous. The dip
of the beds in this place is toward the northwest 10^ to 15°. They seem
but slightly affected by the elevation of the main range on the east, or
of Treasury Mountain on the south. Farther up the stream, which we
shall call Aspen Greek, the dip increases to 45<^, and the nptnrned edges
are lodged against the granite, which, by means of a rather complicated
fault, has been thrust up past the broken edges of the entire series of
earlier sedimentary rocks, bending the edges of the older strata back
and driving them into the softer strata above. In the bottom of the
creek a small portion of the yellow quartzites are exposed, situated as
shown in Section D of the large sheet. This fault would seem to be on
the northern continuation of the line of upheaval to which belongs the
inverted series observed last year about the southern sources of Bock
Creek. Our investigations at that time were extended to within six
miles of this point.
Late in the evening we encamped near timber-line, and on the follow-
ing morning climbed the high granite ridge to our left. We soon found
ourselves in the very midst of the mountains. Snow Mass and Capitol
and Mount Daly rose up magnificently in the east, Sopris stood alone
at the north, and many groups of lofty mountains appeared in the
southwest. All around us were only bare rock and snow. The whole
area is above timber-line, and the sculpture of the mountains is won-
derfully striking and picturesque. The long crooked lines of crests are
connected by subordinate crests, and these all send out sharp, narrow
branching ridges which separate the amphitheater-like hesuls of the
numerous radiating streams. As a rule, these high valleys are wide
and the ridges narrow, so that the country presents the appearance, in
a rude way, of a giant honeycomb. Sopris is connected with Capitol
by the flat ridge of Carboniferous red beds, Capitql with Snow Mass by
a deeply-indented saddle, while south from Snow Mass, the axis crest
continues to Maroon Mountain, thence to the White Rock and Castle
peaks. From the saddle, midway between Capitol and Snow Mass, a
pinnacled ridge extends to the westward between the head-waters of
East Fork or Avalanche Creek and Eook Creek proper. Branches are
thrown out from this between all the small streams, while the chief
crest of the spur continues out to station 22. Stations 24 and 25 were
made about midway on this ridge. Station 24 is the most northerly
summit of the Snow Mass granite, and is eight miles from station 22.
The sedimentary outcrops, which pass just north of Capitol and Daly
peaks, sweep around to the north of this station and turn to the south-
ward, crossing Aspen Creek, as described on the preceding page. Here
the entire series is exposed, there only the Upper Cretaceous and bits
of the Paleozoic rocks in the bed of the creek. The lines Qf outcrop can
be traced between- the two points. The older rocks gradually disappear
as the granite begins to fault up past the broken edges. (See colored
map). This may be regarded as Che farthest northern extension of the
great fault-fold previously mentioned. This fold being a most compli-
cated and int<^re8ting piece of dynamics, calls for a separate analysis,
which I give farther on.
On the 3d we descended Aspen Creek to the main creek and continued
the examination of the Cretaceous section. The black shales, the upper
part of which are exposed in the bluff on the north side of Aspen Creek,
occupy the valley from the base of the bluff to the base of Treasury
i
in
ill ■
I!
IS
n
^<N.
-*'•-.
Fig. B. — Cascadk os Kock Crekk, Coiohaih).
MMO.] TRBASDEY MOUNTAIN. 67
MoantaiD. The dip is at first slight, but before we reach the Lower Cre-
taoeoas, it rises to 30^. The strike is at right angles to the stream-
eonrse, but turusto the south on both sides of the mountain. It appears,
from such examinations as I was able to make, that Treasury Mountain
» a short aDticlinal, or oval shaped qnaquaversal, that seems to have
been produced by some agent associated with great heat, since the high
degree of metamorphism of the entire series up to the Middle Cretaceous
18 quite remarkable. I doubt if the sedimentary measures are entirely
penetrated in any part of the mountain. The Jurassic and Lower Creta-
ceous rocks reach high up the sides of the arch, while the lines of shale-
ODtcrop are ranged around and support the base. The dip is toward
Bock Creek on the east and north, and toward two of its tributaries on
tbe south and west. The only place where the Paleozoic rocks have
been penetrated and exposed is on the east side, where the two branches
of Bock Creek, leaving the Cretaceous synclinal, cut directly into the
side of the anticlinal, passing through the Cretaceous, Jurassic, and Upper
Carboniferous rocks, into theLowerCarboniferous, (see Figure 7;) here, in
a deep, narrow canon, they unite, and turning to the right the resultant
stream follows for some distance along the strike until it reaches the north
end of tbe oval, where it cuts its way out again into the broad depression
eroded from the Cretaceous shales. In passing out over the highly met-
amorphosed beds of the Dakota group, a splendid cascade is formed
with a fall of 500 or 600 feet. Tbe sandstones of this group are so
greatly changed here that it would be impossible to recognize them out-
side of their relations to the overlying strata. They are reduced to a
very hard flinty quartzite, greenish in color and nearly uniform through-
oat The shales above are much hardened, and the Jurassic and other
substrata are so consolidated as to be but a series of flinty quartzites.
For the sake of comparison I present in this connection, Fig. 9, two sec-
tions of the Cretaceous rocks, one made in this locality and the other on
the border of the plains. The Dakota group is everwhere th^ same.
Tbe series of shales are almost identical, and the transitions from shales
to the sandstones above are as like as possible. Palm-leaves and fucoids
are found in the lower* part of these sandstones and in corresponding
horizons.
In the east the lignitic coal is found near the base of tbe sandstones,
while the anthracite coal of the West occurs 2,000feet higher. An an-
alysis of this coal, made by Professor Mallett, demonstrates the fact that
it is of fine quality. (See chapter IX, Dr. Peale's Beport.) The seam is
about four feet thick, but th^ locality is one most difficult of access as
well as remote from any probable market. It certainly cannot be utilized
for many years yet unless the immediate region should prove rich in
iQines, in which case it would be invaluable for smelting purposes.
Between Treasury Mountain and the Snow Mass group there is a long,
narrow Cretaceous valley, produced by an abrupt synclinal fold, in which
the strata are doubled back upon each other. Tlie forces have so pre-
dominated on the east side that the beds on that side are pushed beyond
the vertical and lie atop of the gently inclined strata of the west side,
^e Upper Cretaceous sandstones do not occur in this depression south
of Aspen Creek ; we have, therefore, a double thickness of the black
inhales in the middle of the valle^^, giving in all a thickness of nearly
4i(HM) feet. The shales are followed or supported on either side by the
older strata, in the usual order. The depression produced by this fold
niay be followed the whole length of the Elk range, and separates it from *
tbe West Elk group, producing northern and southern systems of drain-
age.
68 GEOLOGICAL StTRVET OF THE TEBRITOBIES.
THE GREAT FAtJLT FOLD OF THE ELK RANGE.
On September 5th we reached the northern limit of oar last year's
work, and little remained to be done but to examine a few complicated
spots along the main fold of the Elk range. Most of the difficult prob-
lems occur along this fold, between station 24 on the north and Cascade
Greek on the south, and as the axis of the fold is west of the crest of the
range, the complicated parts are cut by the deep transverse valleys of
the western slope and many good sections are exposed. Six of these,
D, E, F, G, H, and I, are given in the main sheet of sections accompany-
ing the map.
It will be observed by reference to the map that the granite, which
is represented by heavy horizontal lines and marked A A, occurs in
two great masses, and that in these masses are the culminating sum-
mits of the range. The northern, which is cut by sections D and £, is
the Snow Mass group, and the southern, cut by sections G, H, and I, is
the White Kock group. At first glance it might seem that these were
separate centers of elevation or upheaval, or at least that they were not
intimately related, but closer examination develops the fact that there
is a line of disturbance of a very marked and extraordinary character
connecting them. Section F cuts this fold at e €, and gives one of its
peculiar phases. But I found that a very large number of sections,
even, could not be made to give a connected idea of so complex a fold.
I have, therefore, prepared the accompanying illustration (Fig. II), in
which the entire fold is given in relief and so placed upon an outlioe
n)ap that the location of the various parts may be easily recognized.
I have carefully kept in view the idea of showing simply the peculiar
foldings of the broken edges of the strata. The granite areas have been
shaded down and the etfects of erosion partially ignored in order to
develop the one idea, and a single convenient horizon, the base of the
Oretadeous, is taken, entirely disincuuibered, for the sake of greater
simplicity.
It should be remembered that this representation is highly artificial ;
that in reality the fold is very obscure, and has but little apparent effect
upon the topography; that it is cut into fragments by ten immense
valleys ; and that its anatomy can only be studied on the steep faces of
the ridges between these vaileys.
It will be seen by reference to the figure and the sections opposite,
that the conditions all along the east side are simple, there being a
gradual and gentle dip from the crest of the range toward the valley of
lioaring Fork, while on the west side there has been a general depres-
sion or downthrow, so to speak, amounting in many places to 7,000 or
8,000 feet; at the same time a combination of movements, principally
lateral, have produced along the axis an immense wrinkle, a fold so
abrupt that the beds are crushed and shattered and the severed edges
shoved past each other, as shown in the drawing and sections be-
tween e and n. It will not be difliicult to imagine that while this was
going on, the plastic mass beneath was assisting the movements and
shaping the results, and that during the process it forced itself, or was
forced, through the fractured line in the two great masses of the Snow
Mass and White Kock groups.
Beginning at the north, I shall give a detailed description. All along
the north face of the Snow Mass group the sedimentary rocks lie in the
usual order upon the granites, with a slight dip toward the north. (See
axis-section, large sheet.) Between Station 24 and Aspen Greek the
granite begins to fault up past the broken edges of the sedimentaiy
^*''^*''^'V
4r
V
"tt
\-
\ ft.
I '■ >
Sandstones
AnthraMt»
Coat Measures
\Sandstone
/ 2000 ft.
I ' I
3=1
\lOOO to 2000 fY.
I Sandstone and
Sfuxles.
^ 20O0 feet
I Skalssk, Slates.
Cfytaceous
aoofti.
•Turaasic
) Sa-tidstoTves
f/i.4^n4t9C' Coal
Sandstonti
loo to 'JooH.
I ! I
Cn
T:nr
soo to 60O feet
Stundstonrs and
SftaZos.
2oooft..
Shales Sc day
No. J Crft4iC4!ouii
t/u-rassir
2^.9
Ji'dattOTis of th& CocJ. Beda to No. 1 Cretaceoua.
Scctw/t I , Wt'.st of the Kanye, Milk MU.
Section ?, EoMt of the Range, ^ Cache la. Poiuir&, orCahon. 6'fy,
M-HniMh MOTO^JTMOOnkPHn. WUHWOTOW. D c
KWOB.) FAULT FOLD OF THE ELK RANGE, 69
sirata, and at Aspen Greek, as previoasly mentioned, only tbe Upper
Cretaeeoas remains in view, with a fragment of primordial rock
at a in tbe deepest part of the valley. South of Aspen Creek for
a few miles the whole series seems to be depressed beneath the sur-
Uobj while the granite peaks on tlie east side of the faoltline rise
to the height of 3,000 feet, making a total displacement of at least
11,000 feet. Soath of 6 there is a high, sharp ridge formed of a series of
almost vertical Carboniferous rooks, which seem to have been carried
up by the granite, or at least to have been left in the present position
by Uie dragging of the fault. In the south end of this ridge the dip
iDereases from 90 to 130 degrees, that is, 45 degrees beyond the vertical,
and Dearly tbe whole series of sedimentary rocks appear in this position
in the side of the canon at c.
Iq the triangular spur between e and ^, a large mass has been carried
back 90 degrees past the vertical, so that the Silurian quartzites oc-
eapy the top of the ridge, and the Cretaceous rocks tbe bottom of the
valley.
1%e fold has been so sharp at e that the beds have been broken off,
and the continued upward movement of the granite has bent the broken
ed|[e8 up, producing a synclinal in the inverted strata.
In this place the belt of granite is quite narrow, so that the relative
positions of the strata on opposite sides can be studied with ease.
The Silurian rooks of the east side outcrop on the summit of the
water-shed of the range at / 2,000 feet above the creek, and since the
lliddle Cretaceous rocks of the west side are depressed to an unknown
depth beneath the creek-bed, we can safely say that there is a vertical
displacement of at least 8,000 feet
The amount of lateral movement (at right angles to the axis of the
tanlt) may be expressed by the difference betwe^i the width of the gran-
ite belt a /and that of the inverted fragment d «, and will hardly fall
sbort of 6,000 feet
SoQth of e the beds gradually rise again from the inverted position,
and a high, narrow ridge is formed of the almost vertical Carboniferous
^ks. This ridge is not above four miles in length, and is connected
with the main range by an irregular cross-ridge that separates the head-
waters of the north and south branches of Sock Creek. The tongue of
^ite that extends southward from Snow Mass along the fault-line is
^nred before reaching this cross-ridge by the overlapping sedimen-
^ I'ocks (at h). Here the greatest confusion occurs, and large masses
oi the rocks, of all ages, are found in the most unheard-of relations to
^ other. The strata of the west side have been depressed and caught
l^^^th the encroaching strata of the east side, and are folded back
^POQ themselves, as seen in the drawing. Figure 11. This peculiar and
*<^ewhat irregular fold may be traced for a distance of six or seven
>|>U6s, and in this distance is cut at right angles by three immense val-
J^ys. The sections exposed in the faces of these are not always distinct,
^t at the same time mak^ it possible to study the peculiar anatomy of
l^^fold.' I observe that in every place where there is an exposure the
Jl'arboniferons rocks of the east side rest upon the upper surfaces of the
^ard sandstones of the Dakota group, and with such a degree of regu-
wty that I was for a long time in doubt as to the identity of the latter,
^nstodying the sectiou exposed on the north side of the valley which
?|^^^ae8 the fault at e, I began near the crest of the main range west of
ipTooD Mountain, and passed down through nearly 3,000 feet of Carbon-
jl^Qs sandstones, limestones, and conglomerates (which have a gen-
^^ dip to the east and undoubtedly belong to the eastern side of the
70 GEOLOGICAL SURVEY OF THE TERRITORIES.
range), bat ou the slope between h and i, I came suddenly opon the
well-known sandstone of No. 1 Cretaceous, lying beneath the Paleozoic
rocks and to all appearances conformable with them. Keeping on at right
angles to the dip, I passed first over the outcropping edges of Jurassic
and Triassic (?) rocks ; then over a ridge of Carboniferous conglom-
erates and limestones, much crushed anfl metamorphosed; and finally,
beneath these still, over a full but much distorted series of Triassic, Juras-
sic, and Cretaceous rocks. The dip rises in places to 70 and 80 degrees,
and the strikes are not quite uniform. I was at first entirely unable to
account for this extraordinary succession of strata, and did not succeed
in solving the i)roblem until I had followed the outcrops across the valley
to the south and discovered in the higher ridge at ; the arch of the fold,
which, on the opposite side of the valley, had been carried away.
It seems that in the first place a great fault occurred, in which there
was a throw sufficient to place the Lower Cretaceous of the west side
opposite the Lower Carboniferous of the east side, and that a powerful
lateral movement had then driven the opposing strata together, the
harder Carboniferous rocks sliding forward upon the upper surface*of
the quartzites of the Dakota group, and at the same time bending them
and portions of the firmer substrata back in a sharp fold, which, from
the continued pressure, has been carried en masse beyond the vertical and
almost severed below by the immense pressure. (See section F, large
sheet.) In the next ridge south, at^', the fold is not so abrupt, and the
ridge m, facing White Rock Creek, there is only a gentle arch of the
strata (see section G, large sheet), while a considerable gap occurs
between the faulted strata in which the granite appears.
At n the infolding ceases, and in the valley at o the strata dip some
forty degrees to the west (section H, large sheet). Toward p they rise
again to the vertical, and at q have been pushed back to forty-five de-
grees past the vertical by a mass of granite, which now lies superim-
posed upon the ridges like so much trachyte.
Before reaching the bed of Teocalli Creek at r, the strata fall back
again almost to the normal horizontal position.
Here the fault forks ) one branch extends southward through «, and
the other turns eastward along the north face of Teocalli Mountain and
continues in a pretty direct course to station 3.
The elevation on the north side of this branch of the fault has been
very great, and has extended over a large area. White Rock and Am-
phitheater Mountains have probably been the highest granitic points,
but the whole mass of the Castle group has been carried up so uniformly
that the Paleozoic rocks lie in an almost horizontal position upon a
plateau-like mass of granite. (See section H, large sheet)
A few miles south of station 3, which is the most southeasterly gran-
ite outcrop of the Castle group, a small pyramidal mass of granite lias
forced its way up through the primordial rocks bordering the granites
of the Sawatch range, producing the summit of Italian peak. Although
this bit of granite seems quite isolated from the previously-described
centers of disturbance, a very marked line of fracture and faulting may
be traced between it and the Castle group, but as the details of this
region have already been given by Drs. fiayden and Peale, I shall con-
tent myself by giving, in conclusion, a brief recapitulation of the more
striking features of the Elk range. Topographically speaking, it is a
spur of the great continental divide, but geologically it is quite inde-
pendent in origin. It trends nearly northwest and southeast, so that
one extremity lies high upon the slopes of the Sawatch range, while the
other extends far out into the low country bordering the Grand River.
I1jr#*i^
^
rig 10.
M.KTEM» mOTO-LTrHOOmrMEn. wammoton. d c
nan. part of the great fault fold of the elk mountains.
«w
Library.
^f I % \tcr »
y
HOLMB8.] SUMM AEY. 7 1
It seems to owe its present conformation to the occurrence of three
nearly parallel lines or belts of displacement, two of depression and one
of elevation.
The depression along the valley of Roaring Fork, which has already
been pi'csented in Fig. 1, is included between the diverging axes of the
two ranges, and exhibits some very curious examples of faulting and
folding.
The elevated belt, which constitutes the range, is about forty miles in
length. It slopes gently toward the depression on the east, but drops off
very abruptly on the west in a great fault-fold. Four considerable areas
of eruptive granite occur along the axis of this belt or zone, and the de
pressions between these contain synclinal folds of the sedimentary beds,
as seen in the longitudinal section given on the large sheet.
It will be noticed, by reference to the transverse sections, that the
axis section, which follows approximately the crests of the range, is
generally to the east of the axis of displacement. The reason of this
will be plain, when it is observed that the entire series of strata rise
gradually from the valley of the Roaring Fork synclinal, until the axis
of displacement is reached, and that the highest points, which would at
first stand along the line of this axis, are now carried back by erosion
iirom one to five miles to the east.
The amount of vertical displacement along the fault-fold, between
Aspen Greek on the northwest, and station 3 on the southeast, does
not fall short of 5,000 feet at any point, and will probably measure 10,000
feet iu one or two places along the west side of the Snow Mass gi'onp.
The depressed belt west of the range, occupied by the valleys of Rock
Creek and Ea«t River, is very intimately associated with the fault-fold,
and has been produced by the downthrow on that side rather than
by any indei)endent folding, as the strata do not rise at all to the west,
except for a few miles along the east face of Treasury Mountain, as seen
iu sections E and F.
On the 11th day of September we fell in with the main party just south
of Italien Mountain, and after spending a few days in the review of the
geology about the headwaters of East River, began our return march to
the East.
f
^y»»^^
^«V
Unibiut
yj
M
•• { 5
Or . . f
- %
EEPOET OF A. C. PEALE, M. D.,
GEOLOGIST OF MIDDLE DIVISION.
1874
r^
REPORT OP A. C. PEALE, M. D., GEOLOGIST OF THE MIDDLE DIVISION.
Washington, D. C, May 16, 1875.
SiB: I have the honor herewith to submit my report as geologist of
the middle division of the United States Geological and Oeographiral
Survey of the Territories for tbe season of 1874.
The report of Mr. Henry Gannett, who was in charge of the division,
will supplement this report, and to it I refer for more detailed informa-
tion in regard to the routes followed, elevation, and topographical fea-
tures of the district assigned us. We left Denver on the 21st of July,
and by the 5th of August had commenced work near the head of the
Eagle River.
On the 1st of November work was suspended and we started tor Den-
ver, reaching that city about the middle of the month. During the
three months we were in the field at work 5,300 square miles were sur-
veyed.
My plan of working was in general the same as during the season of
1873.
Accompanying the topographer in charge to almost all the high sta-
tions, I made sketches of the surrounding country, on which I defined
in colors the boundaries of the various formations. Whenever time
permitted I made detailed sections of the strata.
This report is divided into nine chapters, the first three of which are
devoted to the general geological and topographical features respect-
ively of the valleys of Eagle, Grand, and Gunnison Rivers. The suc-
ceeding chapters give the special and detailed features of the various
formations, and the economical geology of the district. Catalogues of
the minerals and rocks are appended.
The report is accompanied by maps and sections, for which I am
largely indebted to Mr. William H. Holmes and Mr. Henry Gannett. I
have colored the geological formations on a provisional map, reduced by
photography from the original drawing of Mr. Gannett's map of the
district.
The rapidity of preparation and necessary absence during publication
of the report must be my excuse ior any errors that may appear.
In conclusion I wish to express my thanks for the cordial co-opera-
tion of all the members of the party.
With great respect, I remain your obedient servant,
A. C. PEALE.
Dr. P. V. Hayden,
United States Oologiat.
I
I
75
CONVENTIONAL SIGNS USED IN PLATES
J JIT IF J7Z WZl IX JJV
Qzrfrrir.i/e. 9
EZizniznsGzn
f;
aooaaoaoc
Xifr^d/ colore €/ ^€iJt€/s/one,9 ih^f^i'T^r?
i.i.i.i.r.f.r:
Jied aund sfoJies
%«»9iK^09
THi
m
W\Wi^
\¥)maaw»ai
I ■^iA'U
iSiypiiferoLiS aJta/es
TZrzL
J L
J_T
Lij^Itf ^hfi/ts
-Z? or 2*Ar 3 A €g ie
s
JLi
rrt o stones
TV.iT|T||i1,
l-l-l-i-A
^lluvfum
•f ••■*'• ••■• v:- '^^
>*. ■••■I ■> "i • • t
Porfxhy-r^ilCc trcLcJijrfe
» •
XA^o Hie. , tttftM ^^aAs Idia. tx
• • • • •
J* e ecicx
^^o ,90 1 1
^rcA
AT c cr^e
Ill ns.
Library.
/.\
/
Of . . . .
INTRODUCTION.
Tbe territory assigned to the middle division for tbe season of 1873
was thus outlined in the letter of instruction given to Mr. Gannett, who
Tiras in charge, on taking the field :
^^ Tbe boundaries of the area to be mapped by your division (or as
mach of it as the season will allow) are as follows : Commencing at the
intersection of meridian lOO^ 30^ and the Grand River, the line runs
nortbeastward up the Grand River to the junction of the Eagle River;
thence up the Eagle Rive;* to the mouth of Roche Moutonn^e Greek;
theuce westward along the northern boundary of last summer's (1873)
work to its intersection with meridian 107^; thence southward along
the western side of last summer's work, approximately on the 107Hi
meridian, to parallel 38^ 30' ; thence westward on this parallel to the
intersection of meridian 109^ 30' ; and thence northward on this merid-
ian to the intersection of 109^ 30' with Grand River."
This area has an irregular boundary. Grand River, on the north, and
includes between 7,000 and 8,000 square miles, of which about 5,300
square miles were actually worked during the season. The area is
hounded on the west by the Uncompahgre and Gunnison Rivers, leav-
ing the area west of these streams for another season. This gave us a
well-defined natural boundary as our western limit. The greater por-
tion of the area is plateau country, the elevation of which ranges from
9,000 feet to 11,000 feet above sea level. The mountainous portion is
Umited to the southeastern part, along the western edge of the Elk
Mountains. The drainage is comprehended in two systems, viz, that of
the Grand River and that of the Gunnison River.
The entire district is within the limits of the reservation for the Ute
Indians, and a large portion of it had never been visited by white men.
lu 1853 Captain Gunnison, exploring for a route for a Pacific Railroad,
surveyed a belt of country along the river that now bears his name. In
the winter of 1853-'54, Col. John C. Fremont passed over nearly the
same route that Gunnison did. In 1845 Fremont followed the Arkansas
to its head, crossed Tennessee Pass (called Utah Pass by him), to the
Pioey (Eagle), and followed it for some distance, finally crossing to the
Blue (Grand River), and continuing westward. In 1873 Lieutenant
Ruffuer followed Ohio Creek to its head, crossed to the head of Anthra-
cite Creek, and thence to Slate River, going eastward to the Arkansas.
All these were merely reconnaissance surveys, and added but little to
our knowledge of the country outside of their routes. The great mass
of country lying between was unexplored. %»
The general geological features of the district will be given in subse-
quent chapters. The greater portion of the district is covered with
rocks of Tertiary and Cretaceous age, covered in places with lava-
flows.
Mr. Ganuett's report will give all details in regard to the elevations
of iieaks and passes, and topography of the country.
77
y
y.
CHAPTER I.
SUBFAGK GKOLOOY— VALLEY OF EAGLE RIVER.
Baggie Kiver is a branch of Orand Eiver, one of the forks aniting to
form the Colorado. It rises immediately opposite the head of the
Arkansas, and is about sixty-four miles in length. At its head it is
formed by two main branches, one having its source in the Park range,
and tbe other rising in the Sawatch range, which terminates in the
Moantain of the Holy Cross. The Sawatch range, on the western side
of tbe valley of the -Arkansas River, forms the continental divide. North
ot the Holy Cross the range falls off, the water-shed or divide crossing
to the eastward at Tennessee Pass, between the heads of Eagle River and
tbe Arkansas.
Eagle River flows around the northern end of the Sawatch range. Its
g^eoeral course, at first, is a little west of north. Ten miles north of the
ELoly Cross it bends more to the westward, and the general course for
nearly fourteen miles is north 64^ west. It then turns abruptly and
flows* south 78<^ west, which course it holds quite uniformly for about
twenty miles, to its mouth.
Tbe greater part of its drainage is from the south. The entire area
drained by the southern branches is a little over five hundred square
miles. The opposite side of the river was in Mr. Marvine's district, and
wilt no doubt be fully treated of in his report.
Tbe river is a very rapid stream throughout its entire length. The
average fall is 67.2 feet per mile. From Tennessee Pass to the mouth of
Soche-Moutonn6e Creek, the rate is 150 feet, and from here to the head
of tbe second canon 49.4 feet, while from the latter place to the mouth
it is 32.4 feet.
Tbe upper part of Eagle Eiver was partially described in the last
annual report (1873), our division having followed it. as far as Boche-
Montonn^e Creek, for the purpose of ascending the Mountain of the
Holy Cross. In order that this report may be complete I will have to
repeat a portion of the notes on my work of the previous year. For a
distance of about three miles from Tennessee Pass the river is in a
canon*like valley, the hills on either side beiug comparatively low and
rounded. The rocks are granitic, with occasional dikes of volcanic ma-
terial. From this caiion the stream emerges into a broad meadow-like
valley of about four miles in length, in which it is joined by the branch
rising in the Park rauge near Quandary peak.
The valley is three miles in width, the hills on either side of granitic
rock being capped with sedimentary formations, which will be refen-ed
to in more detail in another part of the report. Leaving thiB valley,
the river flows immediately into a canon with steep sides, the trail leav-
ing and crossing to the western branch. A line of outcrop of quartz-
ites crosses the river and follows the summit of the ridge between
the two branches. These beds are, in all probability, primordial. Car-
boniferous beds outcrop on the eastern side of the eastern branch, but
1 deler their description for the present.
7a
80 GEOLOGICAL SURVEY OP THE TERRITORIES.
The western branch is in reality the continnation of the main river,
being twelve miles long. It rises in the Sawatch i*ange, and drains the
country for six miles south of the Mountain of the H0I3' Cross. Its
course at first is north 40^ east, but in the lower two miles it flows almost
at right angles to this, being parallel to the eastern brauch. On the
western side of the stream the hills are gneissic, the sedimentary cap-
ping have been removed by erosion. All the streams joining the river
above the mouth of the Piney on the south and west present abandaot
evidence of intense glacial aetioii. They are parallel to each other, the
general course being north 40^ east. The glaciation was described in the
report for 1873, and I, therefore, simply refer to it here.
Before uniting with the western branch, the eastern fork is joined
by a branch of considerable size having its source in the Park ran^,
opposite Ten-Mile Greek, one of the tributaries of Blue Biver. The
geology about the head of this stream has never as yet been fully inves-
tigated, but I am inclined to think that all the formations, from the
Carboniferous to the Bed Beds, inclusive, will be found along its course.
The Cretaceous beds would scarcely appear until we reach a point
farther north, near Mount Powell. As I mentioned in last year's re-
port,* I think it probable that a fault extends along the western edge
of the Park range, west of Blue Biver.
After the union of the two forks, Eagle Biver enters a deep and inac-
cessible canon of about four miles in length, cut in dark-colored gueissic
rocks, from which it emerges just above the mouth of Boche-Moutonn^e
Creek. The trail keeps high (800 to 1,000 feet) above the level of the
river, on the hills on the eastern side, near the edge of the sedimentary
formations, which are exposed on both sides of the canon. On the
western side there are only patches of quartzite, remnants of the Pots-
dam group. On the eastern side there are other beds, probably of Silurian
age, upon which rest Carboniferous layers, and possibly the Devoniao,
although it seems to be altogether wanting, there being no positive evi-
dence of its existence here. These beds all dip about 10^ to 20^ to the
northeast, the inclination gradually changing more to the north as we
follow the river. In the bluffs on the right-hand side of the river, oppo-
site the mouth of Boche-Moutonn^e Creek, formations from those of Pri*
mordial age to the Permian, or Permo-Carboniferous, are exposed.
This, of course, includes the Devonian doubtfully, for that formation
has not, as yet, been positively identified in Colorado. Just above the
mouth of the creek gneiss is seen on the edge of the river, but as we go
down, higher and higher sedimentary beds gradually form the base of the
bluffs, and below the Piney the line of outcrop of the Carboniferoas
crosses, and still farther down even the Cretaceous shows on both sides,
the strike curving around the end of the range and continuing along
the western side to the Elk Mountains, in our last year's district. On
the west side of the river, as far as the Pine^, there are long spurs, or
ridges, sloping gently at an angle of about 10^, toward the river.
These ridges are capped with quartzite, which I have considered to be
the equivalent of the Potsdam group. These quartzites terminate
within a short distance of the center of the range. Erosion has re-
moved the beds formerly resting upon them, their hardness preserving
them. They are shown in Section B, Plate I.
The creeks, separating these ridges« have their origin in beautiful
meadow-like parks, nestling immediately below the i)eaks in the range,
from whose snow banks they derive their supply of water; thence^ tbef
flow with a comparatively uniform descent to within a short distance of
'Seventh Annual Report, 1873, pa^^e 242.
A"
nALS.] GEOLOGY — EAGLE BIVER. 81
Ea^le, when tbey descend rapidly to its level. The erosion along the
main stream has been much greater for several reasons. In the first
place the beds have a dip from the main range, leaving, perhaps, a sort
of trough between the Sawatch range and the Park range. . This de-
termined the course of the river, which we accordingly tind curving
around the range as the sedimentary formations do. These beds are
also in a great measure made up of sandstones that are comparatively
soft, and yielded readily to the action of water. The river, therefore, is
in a monoclinal rift for a considerable portion of its course.
In thecafion, above the mouth of Eoche-Moatonn^e Creek, the streams
reach the river by falls and cascades.
Tbe slopes are heavily timbered with dense pine forests, and along
the streams are groves of cotton wood, (Po^m/u* treynuloides.) In the
cauon are huge bowlders, which, mingled with the dead and fallen
timber where the forest has been swept by fires, cause great difficulty
in traveling.
At the month of the Piney, a stream coming in from the east, the
river again enters a canon. It is something over a mile in length. At
the head of the canon is a high bluff on the right side, while the op-
posite bank is broken down, allowing the passage of the trail over the
bill, not very far above the level of the water.
On the south side, on the top of the quartzite, (Potsdam ?) are lime-
stones, and, a short distance below, the Carboniferous sandstones cross
tbe river, the angle of inclination being about 25^, a little more to the
northward than in the bluffs opposite Roche-Moutonn^e Creek.
Below the canon the Eagle enters a broad valley, extending for ten
miles, to the head of another canon. This valley will probably average
a mile in width, and is filled with the debris washed ^odq the hills on
either side. It is terraced and covered with a growth of sage-brush,
(Artemuia,) Bordering the river is a narrow belt of alluvium which
videos in the lower part of the valley around two small lake-expan-
sions of the stream. There are beautiful meadows around the lakes.
Tbe lower lake is about a mile long and an eighth of a mile wide, while
tbe upper one is much smaller, being only a little over a half a mile in
length.
Here we found a party of men camped. They were prospecting and
fishing. Eagle Biver abounds in delicious trout of a large size, some
that we measured being sixteen inches in length. Their plan was to
take the fish every week to Oro City, on the Arkanssis River, and sell
tbem. They also claimed to have found gold in some of the streams
coming from the Sawateh range. The gold, if present, is probably de-
rived from the granitic and gueissic rocks that prevail near the heads of
the creeks.
The course of the Eagle through the valley we have just described is
Dorth 780 west. On the southwest side, the long sloping spurs that we
noticed above the Piney still continue. Near the river they are lower,
and, for the most part, grassed over, only an occasional outcrop of lime-
stone or sandstone appearing. On the opposite side are outcrops of
^d sandstone (Triassic?). I have referred to the canon which bounds
the lower end of the valley. It is somewhat curious. On entering it the
^ver changes its course and flows north 45^ west, which direction it keeps
for four miles. It then turns abruptly and flows south 72o west. This
portion of its course in the canon is three miles in length. On the south
^de is a semicircular ridge, extending from the head of the cation to its
foot. It reminds one of a bow, while the river, with its bend, is the
<^rd ready drawn to discharge the arrow. We made two stations on
6h
82 GEOLOGICAL SURVEY OP THE TERRITORIES.
this ridge, which is 1,500 to 2,000 feet above the river. Its rim is
of the saDclstone of No. 1 Cretaceous (Dakota group), which ci
the river at^the head of the canon, almost at right angles to its
the dip beiug in the direction of the stream. On the north side
is a curious spoon-like curve in the strata, shown in Plate II, whicl
be fully explained in Mr. Marviue's report, as it is in his district.|
neath the Cretaceous sandstone, in place, are the Jurassic sbalei
limestones, followed by the Ked Beds, (Tria«sic?) underneath whi
a series of gypsiferous beds, exposed on both sides of the river,
will all be rei'erred to again when I come to speak of the varioi
mations separately.
The river^ on leaving the canon, keeps the course it has there
it reaches the Grand. The valley is about twelve miles long, exti
to within five or six miles of the Grand. It is wide and bordere<
low hills of gypsiferous shales, covered with a growth of cedar ( Jm
occidentMis), Beyond these hills are higher ones, not reaching
timber-line, the basis being red sandstones. The gypsum bills ai
spicnous from their white color and their softness, which causes tl
yield readily to eroding influences. They are therefore mw
up by gullies which forthegreaterportionof theyeararedry,but
storms are the beds of torrents washing down the soft clay. Each
extending into them, fans out into a great number of small gullies.^
shales and sandstones of which they are formed belong to the sam<
zon, viz, Carboniferous or Permo-Carboniferous, as do those menl
as occurring below the Bed Beds above the canon.
It seems as though the Eagle, instead of entering the caiion and ci
its way across the hard sandstone of the Dakota group, shoukll
worn its channel through these softer beds that lie to the southwij
its present course. It might perhaps have done this, but that an
of eruptive rock (basalt), of great hardness, caps the hills south
caiion (see map A), forming a barrier that in all probability deteri
its deflection to the northward. Fig. 1, Plate II, represents a S4
across this area from the Eagle to creek g.
There are two large creeks flowing into the Eagle from the sot
this lower valley. The first or eastern one I will designate as ci
and the other as creek k. They both have their origin in abroad
ridge of red sandstone (Triassic t) which forms the divide or wat<
between Frying-Pan Creek, a tributary of Boaring Fork, and the
of the Eagle. In 1873 we made a station (No. 82), on this ridg^
from it I made a section,* showing the structure of the country as
peare<l to be looking northward. I said, in the report,t that
seemed to be a series of faults and that the section might have
modified when the region should have been more closely studied.
I found this year that the beds I then thought to be Cretaceous,
ing from the color as seen from the st^ition on looking north, are
tlie gypsiferous beds that lie beneath tbe red sandstones. Instei
number of faults, therefore, as shown in the illustration (Fig. 3,
19, Report for 1873), there is simply an exposure of the gypsum
both the places marked '^ Cretaceous," at the head of creek h and it
valley of F^agle Biver. As I mentioned in my notes of last yeai
red sandstones on station 82 dip a few degrees west of north, incli
at a comparatively small angle, which increases as we go norths
On station 8, the dip is in the same direction, as also on station 9.
* Plate 19, Fig. 3, 7th Annual Report, 1873.
t Page 266, 7th Annaal Report, 1873.
JJI'i-KriJ. J
^ ..
-^1
84
GEOLOGICAL SURVEY OF THE TERRITORIES.
low bloff-like wall, teu to twenty feet above the level of the water. It
seems to have come down the ravines in the hills bordering the valley,
and to have spread out like the slag from a furnace. The river seems
to have stopped its progress, for no trace of the rock could be found on
the south side. It seems to have forced the river to the southern side
of the valley, and the force of the water has scooped out the hills, leav-
ing bluifs on that side in which the strata forming the hills are beauti-
fully shown.
i_
r» •*«««>
'.iln
nnj.
CHAPTER 11.
SUBPAOE GEOLOGY — GRAND EIVBR AND ITS TRIBUTARIES.
Grand Eiver rises in Grand Lake, in the northeast corner of Middle
Park, west of Long's Peak, and derives its supply of water near its head
from the Colorado or Front Eange, the divide between Middle and ]Sorth
Parks and the Park range.
It unites with the Green Eiver to form the Colorado, and has a total
leogth of about three hundred and fifty miles, of which one hundred and
fifteen miles is in our district. It rises farther eastward than any other
water in Colorado which flows into the Pacific.
On some maps the name Blue Eiver is given to it, while the name
Grand is applied to the Gunnison and to the Grand proper below the
month of theGunuison. Gunnison* callsit Nah-un-kah-reaor BlueEiver,
and the Gunnison he names the Grand. Blue Eiver, in reality, is in Mid-
dle Park and a branch of the Grand.
The reasons for using the name Grand in preference to Blue are briefly
as follows :
It is really the main stream, being, at the junction of the Gunnison,
twice the size of the latter, andif the nanieis given to the lower portion
it should also be giv'en to the largest stream above. Again, it is so
known all through Colorado and at its head in Middle Park, and will
probably, therefore, always hold good, while the name Blue is restricted
to the branch rising in the divide between the Middle Park and the
South Park, and flowing northward along the eastern side of the Park
range.
la Middle Park Grand Eiver is from forty to fifty miles in length, and
has been fully described by Mr. Marvine in his report for 1873, and
from the Park range to the mouth of Eagle Eiver, a distance of about
forty-five mile'^ in a straight line, it lies within his district for 1874, and
will no doubt be fully reported on by him.
Prom the mouth of the Eagle to the mouth of the Gunnison, it formed
the boundary between the northern and middle districts, and we have
therefore to treat here only of the general features and geology of its
southern drainage in this part of its course. There are three large
branches which I will take up in their order, commencing at the mouth
of the Eagle.
On glancing at the map we notice that there are two general courses
for the streams, the Grand flowing south of west and turning more and
more to the southward as we go west, until at one point it flows almost
dae south, afterward turning to the west before reaching the mouth of
the Gunnison. The courses of the main branches, especially of the
first two, are west of north. The third holds the same general course at
first, but are afterward modified by circumstances that will be explained
&rther on.
'Pacific Railroad Report, vol. ii.
85
86 GEOLOGICAL SURVEY OP THE TEURITORIES.
The area drained by these branches inclades about 1,300 square
miles.
Tbe country included is generally plateau-like in character. This is
more apparent to the westward, and in the divide between the Grand
Biver and the North Fork of the Gunnison. The general elevation of
the plateau is from 9,000 feet to 11,000 feet.
In the eastern portion, from the Eagle River to a short distance west
of Roariug Fork, are rolling hills covered with scrub-oak {Querent atta)^
cotton- woods (Fopulus tremuloides)^ and stunted cedars {Juniperus occi-
dentali^). The latter was most abundant on the lower slopes, aud
seemed to thrive best on soil derived from the breaking down of the
shales in the upper part of the Cretaceous and Tertiary formations. The
rocks throughout this region were mostly of Tertiary age, capped in
places by basalt. The general geology, however, will be dwelt on as
we iiroceed.
The course of the Grand, from the mouth of the Eagle to the month
of Roaring Fork, is south 60^ west. Most of this distance, sixteen miles
in an airline, the river is in caiion, the head of which is a little over three
miles below the Eagle. It is probably impassable to travel, the sides
being very steep. There is no Indian trail following the course of the
river. Mr. Marvine's party kept on the hills some distance back from
the edge on the northern side, and we followed an Indian trail across
the hills to a stream which joins the Grand at the head of the caiion.
This trail seemed to be much used and leads across to Roaring Fork,
which it strikes above the mouth of Rock Creek, a branch rising in the
Elk Mountains.
The valley above the canon is about three and a half miles in length,
and although wider than the valley of the Eagle just above its mouth,
is still comparatively narrow. On the north side are limestone slopes,
and on the south low, rounded hills of the gypsiferous beds. At the
he^d of the canon and forming tbe gateway, as it were, are beds of mas-
sive limestone, probably of Carboniferous age. They dip to the north-
east, inclining about 20^. Farther along in tbe canon there may be out-
crops of older beds, which can be determined only by following the
blufifs close to tbe river. The hills on the south side of the caiion are
ca))ped with a black vesicular basalt, which rests immediately on the
Triassic red sandstones. The dip of these beds I was unable to deter-
mine, but tbey are probably conformable to the layers beneath.
Tbe creek up which the trail led, after leaving the Grand, joins the
river by cutting a small caiion through limestones similar to those at
the head of the canon of the Grand. These beds are somewhat mas-
sive, and above them are blue limestones with interlaminated sand-
stones passing into gray and white sandstones, with yellow and black
shaly beds above. These are beneath the pink gypsiferous beds out-
cropping farther up and corresponding with those on Eagle River.
Still farther up stream the Red Beds appear, the line of outcrop crossing
the creek near its head.
Leaving this creek, we crossed to the waters of Roaring Fork, the first
stream reached being a branch joining it about two miles below the
mouth of Rock Creek. The couhtry between the Grand and Roaring
Fork here is a rolling plateau covered mostly with a growth of scrub-
oak. The plateau is capped with a black vesicular basalt, which in
places is worn away, exposing the red sandstone beneath. The
head of the creek is in canon in which the Cretaceous beds are shown,
dipping to the southwest. Station No. 11 was almost on the line be-
tween the top of the fied Beds and the overlying stata. Farther down
«ALB.l GEOLOGY — ROARING FORK. 87
the creek there are exposures of Cretaceous beds in patches, whose re-
lations I was nnable to determine definitely.
Between the head of the creek and Frying-Pan Creek is a broad-
topped hill or mesa, capped with black vesicular basalt. 1 referred to
this mesa last year,* and then supposed the capping to be trachytic.
The beds beneath it, outcropping on the souch and southeast sides, are
almost horizontal, the sandstone of the Dakota group (Cretaceous No. 1)
appearing on top, the Jurassic beds and Triassic sandstones lying be-
neath in their order. A short distance farther north, on Frying-Pun
Creek, the dip of the red sandstones, which outcrop in massive beds, is
a little east of north at a very slight angle, 5^ to 10^. As we have
already seen, the Cretaceous formations on station 11 dip southwest.
The head of the creek that we are describing, probiibly has its origin in
a synclinal depression, which deepens to the northwest in going down
the creek, and gradually dies out beyond its head on the bioad-topped
hills north of Fiying-Pan. The folds in this region are generally very
gentle, but their axes run in almost every direction. There is so much
eruptive material on top of the sedimentary beds that it is difficult to
trace the connections between the different outcrops. Mr. Marvine
thinks there is a fault running beneath the plateau, betweeii the Grand
and Roaring Fork.
Scattered along the course of the creek, and its branches rising in
ihe plateau, are numerous little meadows. The lower seven miles of
its course the creek is in caiion, which deepens rapidly as we go down.
Tfaerocksatthehead are basaltic, capping the bluffs on either side. They
are present on the hills, or rather plateau, throughout the length of the
caiion. At one point I think Cretaceous shows, although I cannot be
certain, as I did not have time to visit the outcrop. Farther down, the
Red Beds show, and beneath them, at the mouth of the creek, there is a
considerable thickness of the gypsil'erous series.
I will take up next the valley of Roaring Fork. The upper portion
of the valley was described in last year's report, so that this year we
have to do only with the lower part of its course, that below the mouth
of Frying-Pan Creek. There is one point, however, that I wish to refer
to here. When speaking f of the small butte between Maroon Creek
and Roaring Fork, L was at a loss to account for the inversion of the
beds exposed in the butte of which I gave a section. This year
the Elk Mountain region was studied in more detail and a great many
obscure points were explained. In the case mentioned above, Mr. Holmes
foaud a line of faulting extending along the upper side of Roaring Fork
which explained the inversion of the strata.
Below the mouth of Frying-Pan Creek on the right-hand side are low,
rolling hills, the basis of which seems to be the Upper Cretaceous forma-
tion. On the opposite side, however, there are outcrops of red sand-
stones beneath in the bluffs. The Cretaceous strata extend to the gran-
ite of Sopris peak, seeming to rest immediately upon it, there being
nothing showing between until we get on the other faces of the moun-
tain. The geology about the southern part of the i>eak was referred to
last year. Jurassic, Triassic, and Carboniferous layers outcrop on Rock
Greek, but this region will be fully described in other parts of the re-
port, so 1 merely mention it here and to return Roaring Fork.
The course of the latter stream from the month of Frying-Pan* to the
mouth of Rock Creek, a distance of eleven or twelve miles, is north 70^
west, the rate of fall being about fifty feet to the mile. The valley above
•Page 265, report of 1»73. tPage 263, Report 1873.
88 GEOLOGICAL SURVEY OF THE TERRITORIES.
■
the moath of Eock Creek is aboat two miles in width, and beautifully
terraced. The river splits into numerous branches, inclosing islets oq
which are groves of cottonwoods- The terrace blutt's on the north side
are about one hundred feet in height. Kock Creek enters the valley,
emerging from the Elk Mountains, about three miles above its mouth.
After the junction of the two streams, Kock Creek turns and flows north
250 west. Just before it turns, it flows by blutt's of red sandstone, out-
cropping on the north side. They dip 10^ to 20^ a few degrees east of
north. A short distance back of the river they are capped with basalt,
and covered with a growth of low cedars. The hills continue on the
north or northeast side of the river until we reach the Grand. There is
some slight folding at right angles to the river, allowing the gypsiferoas
beds to outcro)) as we go down. It is only a minor fold, for Roariug
Fork occupies the axis of the main fold, which is an anticlinal. Ou
the opposite side of the river there are well-marked hogbacks, in which
the strike is parallel to the course of the river, as is shown also in the
parallel course of the streams draining them. A section through these
hogbacks and across Koariug Fork is shown in section F^ Plate
IV. In tbe hills, farther back, there is basalt on the summits. The
hog-backs extend to within about four miles of the Grand, when the
basaltic capping comes so near the river as to preserve the edge of the
hills and prevent the underlying beds from being eroded. The line of
outcrop also curves slightly to the westward, under the capping, so
that the Cretaceous No. 1, which forms the best defined hog back, is
considerably farther from Eoaring Fork, near the Grand, than it is
near Eock Creek. At this point, then, tbe Red Beds are seen on
top, and beneath a considerable thickness of the gypsiferous strata
outcrops on both sides of the river. Those on the south side bnve
weathered into curious pinnacle and tower like forms of pink, ,> el-
low, gray, and creamy colors. Tbe valley of Roaring Fork is
here comparatively narrow. Tbe river and local driit is terraced,
the terraces in the lower part of the valley being covered with bowld-
ers of black basalt, from the hills back of tbe bog backs. About three
miles and a half above the mouth. Roaring Fork is joined by the. creek
draining the hog-backs, which here cuts across them and iiows along
the upper edge of a terrace that is 200 feet above the level of the river.
The course of-the river here is almost due north until it joins the Grand,
just as the latter emerges from the canon that commences below the
mouth of the Eagle. Tbe exit is through a narrow gorge in the lime-
stones. These limestones continue along the upper side of tbe river,
dipping generally toward the south, at an angle of 20° to 30^. The
inclination is more abrupt near the river, decreasing as we go back, un-
til, on the snmmit of the hills, tbe beds are almost horizontal. On the
south side the Red Beds outcrop, forming blutt's that at some points are
five hundred feet in height, rising in sheer precipices. There are proba-
bly gypsiferous beds beneath, but they are concealed by the local debris,
A short distance back tbe edge of the basaltic mass capping the hills
appears. Its outlines are somewhat ditticult to trace in places, as it is
covered with a growth of scrub oak, and scattered groves of cotton-
woods. The line of outcrop of the Dakota group appears from beneath
the basaltic area, and keeps along the lower side of the river, tbe strike
being north 76^ west. The beds form a series of hog-backs, the contin-
uation of those on Roaring Fork. They extend along the Grand on the
lower side for eight miles, when they cross and stretch away to the north-
west, in an isolated range which gradually dies out in a plateau. A sec-
tion across these hog-backs west of station 17 is shown in Fig. 2, Plate
^^ V
%
[Soarina ^rA
mm
w/i
JLibrary
•\
/
/
Or • . ' '
FEA1B.1 GEOLOGY — GRAND RIVER. 89
lY. The valley of the Grand below the nioath of Roaring Fork is only
about two miles long, the river again entering a canon. At the head of
this caiion tlie Red Beds cross, and are shown on both sides. The river
gradually bends and follows the strike, in 'a monoclinal, rift for six miles,
when it turns again and cuts abruptly across almost at right angles to
the strike, flowing through a valley cut in the soft shaly beds that lie
just above the Dakota group.
This valley is only a few miles in length, and in it the river is joined
by quite a large stream from the north, which flows along the eastern
base of the Cretaceous range, which I have described as ending in the
plateau to the northwest. From this valley the river cuts through tho
stntta at right angles to the strike, and comes out into a broad valley,
through which it flows for fifteen or twenty miles, and enters another
caiion, or rather caiion like valley, cut in a plateau in which the beds
are almost, if not quite, horizontal. This caiion is more or less persist-
ent until the river enters the valley in which it is joined by the Gun-
nison. The general course of the river lor about nineteen or twenty
miles is south TO^-TSo west. At the head of the valley the bluffs are
almost vertical, and, indeed, in some places, the cliffs, as seen in certain
lights, appear to overhang. At the point where the course changes
to the southward, the valley is wider, and the Grand splits, forming
islands in the midst of the river. This is northwest of station 50.
The plateau here, between the Grand and Plateau Creeks, is narrow, and
has in reality degenerated into a ridge from which the basaltic capping
has been removed.
Returning to the valley above the canon, we see that it is from fifteen
to twenty miles in length, and that the drainage on the south is princi-
pally through two streams, one in the eastern portion and the other
(North Mam Creek, see map E) on the western side. They rise in the
plateau forming the divide between them and the head of the North Fork
of the Gunnison. The eastern branch is formed by two streams, whose
courses are almost parallel. Between the East Fork and Roaring Fork
there is a smaller creek (c creek. Grand River), which rises in a
mass of rounded hills, which I referred to w^hen speaking of the hog-
backs on the west side of Roaring Fork. Between this creek and the
plateau south of the caiion theie are several folds, the axes of which
are parallel, each being northwest and southeast.
The rocks underlying the valley are all of Cretaceous age, capped
irregularly in places with basalt, especially on the divide. Here the
strata are almost horizontal, inclining, if at all, only a few degrees
toward the west in the eastern portion.
The line of hog-backs before referred to, extending along the lower
8i(]e of the Grand from station No. 16, through station 18, and cross-
ing the river, forms the side of a synclinal fold, .the axis of which is,
partially at least, occupied by a creek (c. Grand River). The dip of
the strata is southwest, inclining at an angle of about 15^ » this increases
as we go toward the Grand, being about 60° there.
Station 20 is on the opposite side of the fold, the dip of the sandstones
there being northeast at an angle of 16° to 20o. From station No. 19
to 22 there is a mesa covered with basaltic bowlders. I am inclined to
think also that there is a capping of the same material. The bowlders
are derived from the hills near the divide. The mesa is about a mile
wide and slopes gently toward the Grand. It is about 400 feet above
the vallev of the creek at the forks below station No. 19. At station
tion No. 22 it is 800 feet high.
Between the forks of the large creek east of North Mam Creek, the
90 GEOLOGICAL SURVEY OF THE TERRITORIES.
bills are capped with basalt. The elevation of station 24 is 10,642 feet,
and station 25, 9,031 feet. There is but little timber here, the summits
being grassy and park-like. In some few places there are pines, but
cottonwooda are more abundant. In the hills east of station 24, aDdon
the lower slope, there is scrub-oak (Qiiercus aWa) in abundance. The
small creeks rising in the Cretaceous shales we generally found strongly
impregnated with alkali.
The western branch of the creek referred to above, heads in beaatifal
meadows. Its course here is nearly due west. After flowing in t\m
direction for five miles it turns and flows to the northwest, gradually
crossing to the western side of a low, broad anticlinal. The straU on
the east incline 5^ to the northeast, and on tbe opposite side from 5^
to lOo in the opposite direction. Beyond, the beds probably become
horizontal, as seen in the high white clifl's east of station No. 48, on
the edge of the plateau.
In looking down upon this valley from the hills bordering it^ it ap-
pears more open tban it really is, for we find that it has numerous bills
or buttes in which the sandstones outcrop. Tbey are gray, chocolate-
colored, and greenish. We were not able to visit them, but noted them
from the stations on the east side and from the plateau.
We were not on the Grand River in this valley nor on North Mam
Creek, which joins it above the caiiou. North Mam Creek flows along
tbe eastern edge of the plateau from which some of its branches are de-
rived. Its general course is north 15^ east.
The branches of the Grand from the south in the canon valley north
of the plateau are all small and unimportant, simply draining the pla-
teau. Tbe next branch of importance is Plateau Creek flowing into the
Grand 50 or 60 miles below tbe head of the canon. It is a stream of con-
siderable size, deriving its water principally from the mesa divide on the
south, the branches heading in the plateau of station 48, carrying water
only in tbe spring and early summer.
There are two principal streams uniting to form the creek, one (/
creek, map £), having its sources opposite those of tbe northern branches
of the North Fork of the Gunnison, and tbe other {g creek, map E), rising
more to the north and eastward, opposite the head of North Mara Creek.
The branch first mentioned is the largest. It^ course is generally north.
A few miles above its mouth, bowever, it turns abruptly and flows wes^
ward, parallel to the other branch, leaving a flat-topped terrace between.
It rises on tbe divide, in beautiful park-like meadows, among low hills
whose rounded outlines are covered with groves of quaking aspens whose
foliage in the fall of tbe year is of a rich golden hue, contrasting boldly
with the dark green of tbe pines found on the higher points. These
groves abound in game, and are favorite bunting-grounds of the Indians.
We found their trails leading in almost every direction. Near tbe head
of the creek are outcrops of soft sbaly beds covered in some places with
basalt which forms rough points reaching above the general level. In
the valleys tbe soil is made of tbe dSbris from the shales mingled with
pebbles from the erosion of the basaltic layer which once formed a
capping to the plateau. Scattered over it are cbi[)s of chalcedony and
agate. The sedimentary beds are nearly horizontal. As we go down
the valley we find the creek cutting deeper and deeper into the solt
strata, leaving high terraces between the branches. Between camp 44
and camp 45 the river falls 2,583 feet, which is about 200 fe«t per mile.
In the lower part of the valley there are outcrops of solt gray sand-
stones. Tbe terraces are partially covered with scrub-oak, which make
traveling somewhat difficult. The other branch has a much more open
/.
i» — ^
JLibrur.y. j
I
«
«AM.] GEOLOGY — GRAND RIVER — ^PLATEAU CREEK. 91
valley.. It rises among low hills, and has a much more gradual fall to
Its month. It is about 24 miles in length, and forms a portion of the
boundary-line of the plateau of station 48. Between the parallel por-
tions of the two streams just described there is a terrace, the height of
which is about 80 feet, at the bend of the first branch. It is about a
mile wide here and slopes to the forks, where it terminates in a point,
the entire length of the bench being about seven miles. It is covered
with good bunch-grass, and has evidently been used by the Indians as a
grazing-gronnd tor cattle. The plateau between this creek and the
Grand Biver is approximately triangular in shape, the base being on the
eastern side. Here it is 15 miles in width. To the west it gradually
terminates in a ridge, which extends between the two streams. Its
length is 15 miles, and its mean elevation, where the general level is
best preserved, is about 10,200 feet. It was once, doubtless, continuous
with the mesa or plateau which still exists to the southward. Erosion
has isolated it. The covering of basalt which once covered it has been
partially removed. The remnants left reach from 200 to 250 feet above the
general level, forming monument-like points that are visible from a great
distance. Station 48 was located on one of these points, a conical mass
248 feet high. The eastern edge of the plateau, as I have already men-
tioned, has steep blu£fs, overlooking a broad valley. On the north side,
also, are bluifs, which as we go down the Grand become less steep, a num-
ber of small streams cutting them into small hills. Toward the eastern
side the beds are nearly horizontal, but as we go west we find that there
is a slight dip to the east, or perhaps a little north of east. The south-
ern side of the plateau, near station 48, has a number of creeks draining
it, the courses of which are nearly parallel, flowing south. Between them
are sharp ridges, at the base of which gray and pinkish sandstones
outcrop. On top are light clayey beds and interlaminated hardened
shales, weathering a white color, thus giving the bluffs a unique appear-
ance, as s(^n from a distance. Underneath the basalt, the beds are
eoncealed even on the edges of the plateau. As we go down the creek
the valley widens on both sides. On the south are drift-covered ter-
races sloping from the divide. On the north side are low bluffs, close
to the river, in which pink and yellowish strata outcrop. These beds
are cut into terraces, beyond which are bluffs of variegated sandstones,
passing above into light colored shales. On the latter, station 50 is
located. From station 50 to the Grand the descent is at first rather
abrupt. Then there is a gradual slope broken up by the drainage into
low buttes. The Grand has a broad bottom, through which it flows
sluggishly.
South of the station the country is very nearly the same. There are
magnificent exposures of the strata, which are inclined but slightly. On
the north side of Plateau Greek are bluffs of sandstone, through which
the stream cuts rapidly to soft shales, which weather in the most pecu-
liar manner, as shown in one of the illustrations, Plate Y. Above the
black argillaceous columns are yellow sandstones, and the dSbria from
them has fallen down, capping the summits of the pillars. Below, still
lower beds are shown, until a belt of red sandstone is seen opposite
Mef:a(a) Creek. It here enters a canon, in which it keeps until it joins the
Grand. Almost all the creeks in this region cut profound canons ; even
the smallest rivulets cut gullies from eight to twenty feet deep.
The terraces are covered with basaltic bowlders, and are almost des-
titute of vegetation. Good grass, however, is found in the alluvial bot-
toms bordering the creek. Scrub-oak and stunted cedars are fonnd on the
liills. The caiiou on Plateau Creek is eight m.les long. Below its moath|
92 GEOLOGICAL SURVEY OP THE TERRITORIES.
the Grand and its branches cut fearfal-looking chasms in the soft rocks.
Looking down upon them it is hard to trace the courses of the streams,
as it appears to be an inextricable maze of gorges.
There is great variety in the colors 5 reds, greens, grays, yellows,
mingle with chocolate-browns, and white, in parallel lines, which repeat
themselves in the diflPerent layers.
At the head of the caiion of Plateau Creek the Indian trail we had
been following leaves the creek, goes up Mesa Creek, and skirting the
edge of the mesa, leads down into the valley of the Gunnison.
The course of Grand River below the mouth of Plateau Creek is gen-
erally southwest, and sometimes due south.
It flows in this direction until it comes out into the broad valley, in
which it is joined by the Gunnison. It emerges from the canon by cut-
ting its way across a line of hog-backs, almost at right angles U) the
strike of the strata, the beds dipping about northeast at an angle of 10^
to 150.
Plate VI represents the bluff on the north side of the river, as it comes
from the canon into the broad valley.
The numbers in the following section correspond with those in the
illustration.
BASE.
1. Black and yellow shaly beds.
2. Yellow sandstone.
3. Yellow shaly beds.
4. Sandstones.
5. Shales.
6. Sandstone with pinkish hue.
This section was made from the opposite side of the Grand, and conld
not, therefore, be made in greater detail. The beds were measured by
angles taken with the gradienter. The height of the bluff as^hus deter-
mined is 1,890 feet. On the south side of the river the inclination of ;
the beds causes them to disappear, while higher ones show beneath the j
basalt of the mesa. The slopes, reaching from the edge of the mesa iu |
terraces, are covered with basaltic bowlders, among which we found \
numbers of moss-agates (none of good quality, however) and pieces of |
chalcedony. !
West of the line of hog-backs, which extend toward the northwest
from the Grand, the valley is about eighteen miles in width, reaching to
the northwest as far as could be seen. Near the Grand, before the
Gunnison comes in, it is very fiat and covered with spots of alkali. On
the south side of the Grand, in the angle between it and the Gunnison,
are terraces, the first of which is one hundred feet high, and the second
nearly two hundred feet. The contrast between the two rivers is quite
marked. The Grand has nearly twice the volume of the Gunnison, and
and carries a vast quantity of mud with it. Wherever we reached the
Grand throughout the entire season it was muddy. The reason is, that
along the river there are many exposures of soft shales and clays.
The Gunnison, on the other hand, is a clear stream, and remains so except
when there are heavy rains, when it becomes very turbid in the lower
portion of its course.
The divide between the Grand and Gunnison Bivers has been so often
referred to in this chapter that only a few more words are necessary to
complete its description. In the Elk Mountains the line of the water-
shed is very irregular, the mountains rising in sharp peaks, at the bases
of which the streams head in amphitheaters, sharp ridges connecting
tu
Is
r
V
vv;-si
<^o>
, N
f
i
N N
\
J-
'■i^^x
n
%
/
/
/
li ii/i/j
13
ft
x
»i^"t.] GEOLOGY — DIVIDE WEST OF ELK MOUNTAINS. 93
the peaks and separating the various streams. This portion of the
divide.*, however, was in the district of 1873, and we have to do here with
the portion west of the Elk Mountains, where it presents characters en-
tirely different, being mostly a plateau, from the fact that the beds un-
derlying it are almost horizontal and covered with allow of basalt. The
plateaa character is best shown toward the west, where the basaltic
capping is for the most part intact.
West of Eock Creek, at the head of the !N"orth Fork of the Gunnison,
the plateau is broken into low rolling hills, of which the general level
is very nearly the same. The basaltic capping here is very irregular
and difficult to define, as a great portion of it has been removed by ero-
sion. The hills and also the beds of the streams are covered with
round masses of the rock. At station 45 there is more basalt in place.
The streams rising near have their origin in small lakes. All over the
plateau these lakelets may be found, and along the creeks are beautiful
meadows. The timber on the plateau is pine and quaking aspens {Popu-
lus iremuloides). There is good grass in most of the valleys. The
western edge of the plateau is somewhat irregular but sharply defined,
forming a bluff edge of from two hundred to four hundred feet in height.
It is underlaid with sandstones, as will be shown in the sections given
in a subsequent portion of the report.
CHAPTER III.
SUEPACE GEOLOGY— GUNNISON BIVEB AND ITS TBIBtTTABISS.
Gannison Eiver is the principal branch of the Grand, on the sooth
side. It rises on the western side of the Sawatch range, opposite the
Arkansas River, and on the soathern side of the Elk Moautains, oppo-
site Roaring Fork. Its total course has a length of about two hundred
miles, the average rate of fall per mile being about thirty feet. In
Gunnison's and in Fremont's reports it is called the Grand. In the
West, however, it is now known as the Gunnison River, the name
Grand being given to the principal stream, as already mentioned in a
previous chapter. The principal branches of the Gunnison on the
south are Cochetopa Creek, Lake Creek, Cebolla Creek, and Dneom-
pahgre River. Those on the north, in our district of this year, are Ohio
Creek, Smith's Fork, and the North Fork. The entire area drained by
all the branches on the north is about twenty-six hundred square miles.
From the mouth of Cochetopa Creek, the Gunnison flows a few degrees
south of west, to Lake Fork ; here it changes and flows west, gradually
turning to the northwest until it is opposite station 80, a distance of
nearly thirty miles ; when it again turns and flows nearly due north to
the mouth of the North Fork; where it turns abruptly and flows west to
the head of what the Indians call Una weep CaQon. * It« course thence
to its mouth is generally northwest.
There are three large cauons and several small ones in the course of
the river, which will be described as we reach them in going down the
stream. The upper one is in granitic rocks, and was described last
year. The drainage of the streams uniting to form the Gunnison near
its head flows in two directions, viz, southeast or south-southeast, and
southwest. In this part of its course it is within last year's district,
and will be found described in the report for 1873.
Our work last year extended as far west as Slate River, and we com-
mence this year, therefore, with Ohio Creek, the next stream coming into
the Gunnison on the north side.
In an airline, from the head of Ohio Creek to its mouth the distance
is twenty-two miles. The actual length, however, is nearer thirty miles.
It has its origin in a group of isolated peaks that mark the termination
of the Elk Mountains to the westward. Its sources are opposite those
of Slate River on the north and east, and those of Anthracite Creek, a
tributary of the North Fork of the Gunnison, on the northwest. It has
two forks which unite below a high sugar-loaf peak of porphyritic
trachyte, station 30. The western branches have their origin in a group
of mountains made up almost entirely of breccia, which in all probability
rests on sandstones of Cretaceous age.
The most northern of these streams flows along the southern edge of
a short range of sharp peaks, whose slopes are destitute of timber, and
which form a serrated edge along the summit. This mass is composed
of porphyritic trachyte and forms a portion of the divide between
■ » ■ ' -
* Pacific Railroad Report, yol. ii.
94
HULR.]' GEOLOGY OHIO CREEK GUNNISON RIVER. 95
Ohio Greek and Anthracite Creek. A trail crosses through alow pass
from the head of the latter creek and keeps down Ohio Creek and then
follows np Cochetopa Creek to the Los Piuos agency. This is one of
the main Indian lodge-pole trails, connecting LosPinos with the White
River agency.
Between East Eiver and Ohio Creek are two mesas, isolated one from
the other and underlaid by Cretaceous shales and sandstones. These
mesas are composed of trachyte, judging from the debris covering the
slopes west of Ohio Creek. The trachyte is probably of the same char-
acter as that on the opposite side of East Eiver noted in last year's re-
port,* a light purplish rock. As I have already mentioned, the hills on
the west side of Ohio Creek are made up almost entirely of breccia.
I will refer to it particularly in a subsequent portion of the report. I
think Judging from several outcrops seen on some of the western branches
of the creek, that it rests throughout the greater part of its extent upon
sandstones.
The western branches rise in these hills and cut deeply into the brec-
cia, which seems to yield readily to the action of water. It appears to
be in layers, and erosion has worn it into fantastic forms. In places, there
are castellated masses from which towers and minarets rise 3 while in
othei*s, huge buttresses stand out prominently against the sky. Station
1^0. 31 is situateil in the midst of this mass of breccia. (See map D).
The valley of Ohio Creek is from a mile to two miles in width and
has a beautiful grassy bottom, with groves of cottonwoods. The hills
on the west are heavily timbered with pines, extending down the ridges
hetween the branches. On the lower slopes near the creek there is sage-
brnsh {Artemutia).
The valley of the Gunnison above the mouth of Ohio Creek is very
wide, extending from a short distance below the mouth of Slate River
to Cochetopa Creek, a distance often or twelve miles. It is from four to
seven miles in width. The river-bottom in places seems to be quite
fertile, and at one place we found a garden in which potatoes, beans,
turnips, cabbage, and lettuce had been successfully raised during the
sea8on.
The southeast side of the valley, reaching toward Cochetopa Creek,
is rather sterile-looking, there being but little soil. It is very level and
covered with pebbles derived from the Elk Mountains. There is a sparse
growth of grass and low sagebrush. The Gunnison here is a rapid and
verv clear stream of a hundred or a hundred aKd filtv feet width. It
•r' «
keeps close to the bluffs of breccia below the mouth of Ohio Creek.
This valley is the site of a new town called Gunnison City. There
were half a dozen log-cabins, most of them in an unfinished state and
without inhabitants. The only persons we found living in the valley
were the two men who hfkve charge of the cattle for the Indians of Los
Pinos agency. They were at the cattle-camp, a short distance above
Cochetopa Creek. Below Cochetopa ( ^reek the valley again expands
into a grassy meadow, from which the river enters a canon. Men from
the agency were busy cutting grass in this meadow while we were
there. The hay made is for the use of the agency aud the cattle-camp.
The cattle are allowed to run wild among the hills throughout the year
and seem to do well. The country is much better adapted to stock-rais-
ing than for agricultural purposes. The elevation of the cattle-camp is
7,743 feet.
The lower valley is about four miles long and two miles wide in its
greatest width. On the northern side the breccia forms the boundary,
' Page 249, Report 1873.
96 GEOLOGICAL SURVEY OF THE TEERITOEIES.
trachyte capping it as we go toward the hills. On the south side the
rocks are gueissic, as they also are in the caiion. At the upper end of
the valley, on the north side, is an outcrop of soft yellowish gray sand-
stone. Farther down the breccia, instead of resting on this sandstone,
appears to be directly upon the schists. At station 71, however, between
the schists and the breccia there is a belt of sandstone that seems to
have been metamorphosed. Above the breccia there is a capping of
trachyte.
The canon is only about a mile and a half in length, and in it the river
has rather a tortuous course, flowing at first south of west and afterwards
north of west. The walls are not very high, never exceeding 300 feet
Below, the river is in another valley similar to the one above. Tbis,
however, is not as large, being only two miles long and a mile wide in
the widest portion. It is not so well grassed as the valley above. The
schists still compose the hills on the lower side, while on the north there
are sandstones, breccia, and trachyte in long mesa like ridges that
extend from the margin of the valley toward the hills in which station
31 is situated.
Leaving this valley the river again goes into canon and keeps so
almost all the way to the mouth of the Lake Fork, broken only by small
and unimportant valleys. The rocks in which the river-channel lies are
schists, and the. walla never exceed about one hundred and fifty feet
in height. This granitic rock forms a narrow strip, leaving a bench or
shelf on both sides of the river, reaching back to the edge of the blufis.
On top of the schists, forming the base of the blutf, are the sand-
stones that probably belong to the Dakota group. As we proceed down
the river we find on top of these, black and yellow shales, above which
is the breccia to which I have so frequently referred in this chapter.
This, in a great many places, has weathered into sharp pinnacles and
towers. It is capped with obsidian and trachyte.
A section of thebluffs will be given in another place, when the differ-
ent layers will be particularly described.
These bluffs are on both sides of the river, and form the edge of the
mesas that are so characteristic of this part of the valley of the Gun-
nison, extending back from the river on both sides.
Below station 71 the top of the mesa is about 500 feet above the
river-level, and at station 73 it lias increased to 1,230 feet, the general
surface really remaining at the same level on both sides, while the
river in its progress has cut deeper and deeper, making the bluffs nearly
twice as high. This height is still greater farther below, aa we will find
when we speak of the canon.
The streams joining the Gunnison cut deeply into the surface, divid-
ing the original mesa into many others. The canons thus formed have
almost perpendicular walls. There appeared* to be more than one
layer of the trachyte, for, from the edge of the mesa a higher outcrop
can be seen. I was notable this year to determiqedefinitely the relations
between the trachytic flows and the breccia on the mountainous mass
around station 31. Another year I hope to explain it.
Above the mouth of the Lake Fork, the Gunnison flows through a
small open valley covered with grass and sage-brush, in which it is
joined by a branch of some size from the north. From this valley the
river plunges into the largest caiion in its entire course. Lake Fork is
itself in a deep canon, cut through dark, micaceous schists, and until
one comes to the edge of the gorge, he has no idea of its size or extent.
Gunnison's wagon-trail is obliged to cross it a long way back from the
river, and come down the stream on the opposite side.
' 5, i '
r * '- ^- *
..-'
\
96 GEOLOGICAL SURVEY OF THE TERRITORIES.
trachyte capping it as we go toward the hills. On the south side (he
rocks are gueissic, as they also are in the caHon. At the upper end of
the valley, on the north side, is an outcrop of soft yellowish gray sand-
stone. Farther down the breccia, instead of resting on this sandstone,
appears to be directly upon the schists. At station 71, however, between
the schists and the breccia there is a belt of sandstone that seems to
have been metamorphosed. Above the breccia there is a capping of
trachyte.
The caiion is only about a mile and a half in length, and in it the river
has rather a tortuous course, flowing at first south of west and afterwards
north of west. The walls are not very high, never exceeding 300 feet
Below, the river is in another valley similar to the one above. This,
however, is not as large, being only two miles long and a mile wide in
the widest portion. It is not so well grassed as the valley above- The
schists still compose the hills on the lower side, while on the north there
are sandstones, breccia, and trachyte in long mesa like ridges that
extend from the margin of the valley toward the hills in which station
31 is situated.
Leaving this valley the river again goes into canon and keeps so
almost all the way to the mouth of the Lake Fork, broken only by small
and unimportant valleys. The rocks in which the river-channel lies are
schists, and the. walla never exceed about one hundred and fifty feet
in height. This granitic rock forms a narrow strip, leaving a bench or
shelf on both sides of the river, reaching back to tbe edge of the blufis.
On top of the schists, forming the base of the bluif, are the sand-
stones that probably belong to the Dakota group. As we proceed down
tbe river we find on top of these, black and yellow shales, above which
is the breccia to which I have so frequently referred in this chapter.
This, in a great many places, has weathered into sharp pinnacles and
towers. It is capped with obsidian and trachyte.
A section of thebluffs will be given in another place, when the differ*
ent layers will be particularly described.
These bluffs are on both sides of the river, and form the edge of tbe
mesas that are so characteristic of this part of the valley of the Gun-
nison, extending back from the river on both sides.
Below station 71 the top of the mesa is about 500 feet above tbe
river-level, and at station 73 it lias increased to 1,2-30 feet, the general
surface really remaining at the same level on both sides, while the
river in its progress has cut deeper and deeper, making the bluffs nearly
twice as high. This height is still greater farther below, as we will find
when we speak of the canon.
Tbe streams joining the Gunnison cut deeply into the surface, divid-
ing the original mesa into many others. The canons thus formed have
almost perpendicular walls. There appeared to be more than one
layer of the trachyte, for, from the edge of the mesa a higher outcrop
can be seen. I was notable this year to determiqedefinitely therelatious
between the trachytic flows and the breccia on the mountainous mass
around station 31. Another year I hope to explain it.
Above the mouth of the Lake Fork, the Gunnison flows through a
small open valley covered with grass and sage-brush, in which it is
joined by a branch of some size from the north. From this valley the
river plunges into the largest caiion in its entire course. Lake Fork is
itself in a deep canon, cut through dark, micaceous schists, and until
one comes to the edge of the gorge, he has no idea of its size or extent.
Gunnison's wagon-trail is obliged to cross it a long way back from the
river, and come down the stream on the opposite side.
V ■
. i-
• ' i.
'. «■// >' 1/
(trtj
f s •'• *- \
^^t^^T^OJR}
KALE.1 GEOLOGY — GUNNISON CANON — SMITH'S FORK. 97
The country between Lake Fork and the Uncompabgre River is rongb
and ragged. The streams cat deep canons to join the Oannison.
Moantain Creek, Blae Creek, and Cebolla Creek are the principal streams
draining this region. Blae Creek, to which 1 have jast referred, is placed
ou Gunnison's map, as a branch of Cebolla, whereas it is a tributary
of the Gunnison.
The mesas are found on Mountain Creek, and until we reach Cebolla
creek. Here we meet with cretaceous shales, seeming to be horizontal,
and resting on granite. The granite in places has trachyte resting on
it I noticed it on the hills east of Cebolla Creek.
The great canon of the Gunnison is about fifty miles long. In it the
course of the river at first is west ; it gradually changes toward the
north, and at station 80 flows northwest, gradually becoming due north,
which course it keeps rather uniformly to the mouth of the North Fork.
From the head of the canon to the mouth of Smith's Fork the
main portion is cut in dark micaceous schists. It has its great-
est depth, perhaps, opposite station 77 ; the height from the water to
the top of the mesa on which the station was located being about
3,000 feet. The granitic portion is about 2,000 feet deep. It was,
of course, impossible to reach the edge of the river while in the cation,
80 that these figures are not perfectly accurate. They are obtained
by comparing the heights of stations 77 and 78 with that of camp
No. 53, on Cebolla Creek, about one mile above its mouth, and allow-
ing for the fall of the river between the two points. The error, if any,
would, therefore, be very small and in favor of greater depth.
The section across the river, through stations 77 and 78, is shown in
Figure 2, Plate VI I. On the west* side of the river is a plateau about
four miles in width and thirteen miles long. Its elevation above
the river is 2,500 to 3,000 feet. It is composed of schists, and the top
seems to have a gentle slope to the eastward. It seems to have had in
places a capping of trachyte.
East of Cebolla Creek, on the granite hills, a portion of this trachyte
still remains. To the northward the plateau runs to apoiut, the termina-
tion being marked by ahigh conical point of granite. Beyond this, are red
sandstones (Triassic), with superimposed Jurassic and Cretaceous strata,
as seen from station No. 80, on the opposite sideof the river. Fig. 1, Plate
VII, shows a section through station 80. It will be seen that the granite
forms a sort of shelf along the river, on which the sedimentary forma-
tions rest, having bluff-like edges a short distance farther back. These
beds incline at a small angle (about 5^), causing the country to slope
gently toward Smith's Fork, which here flows almost parallel to the
Oannison. The illustration. Fig. 1, carries the section across Smith's
Fork. Beneath station 80 is an outcrop of the Bed Beds. Where the
section crosses Smith's Fork, the latter stream does not cut below the
Dakota group (No. 1). Near the mouth, however, it cuts through the
Bed Beds reaching the granite.
Smith's Fork joins the Gunnison as the latter emerges from the gran-
itic portion of its canon, and cut« across the strata into the Cretaceous
sandstones. It rises in the group of tra^hytic peaks that I have already
referred to as terminating the Elk Mountains to the westward. Before
it leaves these peaks there are outcrops of Cretaceous shales seen near
the water's edge, on the main creek at flrst, but afterward spreading out
and covering wider areas. After it is fairly out of the mountains it flows
across the Upper Cretaceous formation, and gradually cuts throagh the
sandstone of No. 1, which forms bluffs extending along its course from
the mouth of the Southern Fork to the mouth. (See map B).
7 H
100 GEOLOGICAL SURVEY -.OP THE TEBRITORIES.
Grand, immediately opposite tbe plateau in which station 48 was lo-
cated. Its coarse is nearly south, on a line with Coal Creek. The valley
is comparatively narrow, there being but tew open bottoms along its
course. The slopes of the hills on either side are well timbered with
pines and cottonwoods. Near the head of the main creek there ai*e
large bowlders of a black basalt, derived, in all probability, from tbe
layer which once covered the entire divide. While on this creek we
met a party of prospectors, who said they had found indications of gold
along the stream, but not in any very great quantky.
The divide between Bock Creek and this branch of the North Fork is
a sharp ridge of Cretaceous sandstones, reaching above the timber-line.
The strata dip about 15^ to the west, the angle decreasing on crossing
theNorth Fork, until they becomealmosthorizontal in theplateau divide
between North Fork of the Gunnison and Grand Biver. Station 26 was
located on this ridge. The lines of outcrop between the station and
Sophs peak are the prolongation of the hog-backs on the west side of
Eoaring Fork.
The rock on the summit of station 26 is a compact greenish-gray
sandstone, somewhat laminated, and containing in the lower part frag-
ments of stems and leaves, and particles of carbonaceous mat<erial. The
most careful search revealed nothing perfect enough for identification. Be-
low this sandstone is a narrow band of dark-colored, very compact lime-
stone, of a reddish-brown color on the weathered surfaces. Next below is
a coarse textured, soft, gray sandstone, which seemed to continue to the
base of the amphitheater which the station overlooked.
Near the base of the slope we ascended, I noticed an outcrop of con-
glomerate in which the pebbles were of a rock very much like that form-
ing the nucleus of the Elk Mountains. The matrix was siliceous.
What the relations of this bed were to the sandstones I could not de-
termine, as the slopes were covered with a heavy growth of timber, and
tbe underlying beds were for the most part covered with d6hr%s. The
pebbles were rounded and evidently water- worn.
South of station 26 the strike curves to the eastward, the dip changing
more and more toward the southwest. The line of outcrop of the Creta-
ceous beds crosses Rock Creek into the Elk Mountains, where they become
very much faulted and upturned. In this portion of the Elk Mountains
Dr. Hayden made a more detailed survey, and to his report and the re-
port of Mr. Holmes, the reader is referred for the geology of Bock Creek
and the adjacent peaks.
Station ^ was located south of station 26 on one of a group of high
peaks, rising from a mass of trachyte resembling that composing the
mountains between Anthracite Creek and the head of Ohio Creek near
station 32.
The western slope of this ^mass is extremely steep, the sandstone
reaching to the base , almost horizontal in position. At the northern
end, however, as seen from a distance, the strata appear to dip to the
northeast at an angle of about 40^, so that there would seem to be a
synclinal fold between this point and the ridge, extending from station
26. A branch of North Fork rises here and flows nearly due west. Near
its mouth the beds are also inclined towards the northwest, although
the angle is only about 6^.
At the southern end of the mass in which station 33 is situated, on
Anthracite Creek, the sandstones are tipped up, dipping north 54^ west
atanangleofl5^. Dikesof trachyte penetrate thesandstones. The branch
of North Fork that we have just been considering, after the union of the
i '* ^ / *
JJhrary^
\
/
Or f-^f
^ %
PSAUtj GEOLOGY — ^NORTH FORK OP THE GUNNISON. ^ 101
streams heading in the plateau, flows for a short distance through a
beantifal grassy valley, &om which the country on the west rises in a
plateau which is timbered on the slopes.
At the lower end of the valley the stream gradually cuts deeper and
deeper into the i^ndstones, until, at the point where it meets Anthracite
Greek, it is about a thousand feet below the general level. All the
branches here, even the smallest, cut these canons, leaving mesas or tables
between, in which the strata are nearly horizontal, thus giving them
about the same general level.
After the union of the two main creeks, the North Fork flows a little
south of west, almost at right angles to the former courses, in a canon
which is from 1,500 to 2,000 feet deep. This caiion is about fifteen miles
long. In the lower part the river gradually turns to the southward,
finally emerging into a rather broad, open valley extending on the lower
side to the foot of the hills on which stations 38 and 39 are located.
The valley becomes wider as we go toward Smith's Fork. It is compara-
tively open, being broken only by low hills or buttes of yellowish and
gray shales, all belonging to the Cretaceous formation. These buttes
have a scattered growth of stunted cedars and sage-brush. The soil is
impregnated with alkali, and generally sterile. - The small streams cut
deep guUeys in the soft beds. As the river emerges from the canon the
mesas on the south side end abruptly in steep blufi's, just north of
stiition 39. Stations 38 and 39 belong to the tracbytic group, to which
I have already so often referred. They are beautiful examples of moun-
tain forms, rising in sharp conical points. Station 38 risers 4,000 feet
above the general level of the valley which it overlooks. As already
described, there is a gradual slope from the Gunnison to Smith's Fork, the
sandstone of the Dakota group forming the floor. Crossing Smith's Fork,
the softer beds, which we have already described, form lines of buttes.
Along the North Fork there are outcrops of black shales, in which the
general dip is to the northeast. On the north side of the river is a series
of terraces sloping from the basaltic-capped mesa which here forms the
divide between the Grand and Gunnison Rivers.
Leaving the mesa canon the North Fork turns still more toward the
south, and flows southwest to within about four miles of its mouth, when
its course becomes due west. In this valley the river winds in graceful
curves, outlined in the most distinct manner, as seen from the moun-
tains and plateau, by the fringes of cottonwoods on its banks. Just
before it turns to the westward it enters a cation. The walls, at
first, are mere bluffs, cut in the black shales that lie immediately above
the Dakota sandstone. By the time it joins the Gunnison it has cut
pretty deeply into the Dakota group. The river in this part of its
course is parallel with Smith's Fork, and joins the Gunnison in the caiion
ftt right angles to the former course of that stream. The Gunnison,
however, turns and flows to the westward in the direct line of the North
Pork.
This part of the canon of the Gunnison is ten miles in length and with
^alls from 400 to 500 feet high. Although in many places the bluffs rise
in sheer precipices from the river's edge, in others there are alluvial
bottoms, sometimes on one side and sometimes on the other. The general
course is about due west.
Fig. 3, Plate YIII, represents a section across the Gunnison through
the Une E F, on map B. At a it cuts the river just above the mouth of
Smith's Fork, before it leaves the granitic canon, and at d it cuts the
river below the mouth of the North Fork. It will be seen that there is
102 • ' GEOLOGICAL SURVEY OF THE TERRITOBIES.
a slight synclinal fold between c and <f, which is more marked farther
west, as shown in Fig. 2, which is a section across the Gunnison just
before it leaves the canon, on the line G H. The following is the sec-
tion represented in Fig. 3, the figures corresponding with section L.
SECTION.
1. Granite reaching to edge of the river.
2. Bed sandstone (Triamef).
3. Greenish and gray shales and sandstones (Jurassic fj.
4. Shaly sandstones. ) n^i.^*^ ^-^^.^^
6. Massive sandstones. } ^^*^*^ ^''''''^'
6. Laminated sandstones and black shales.
7. Black shales. > Cretaceous.
8. Dark yellow shales.
9. Light yellow and gray beds.
10. Terrace with light-colored shales. j
At a in Fig. 2, Plate YIII, the strata are seen to be curved abruptly,
the river occupying the axis of an anticlinal fold. This is at the point
where it leaves the canon. The fold, however, is not simply a north
and south fold, for, aa we see in Fig. 1, Plate YIII, there is folding
east and west. This is the main fold, or rather the termination of the
anticlinal fold, the axis of which the Gunnison follows in the canon
above Smith's Fork.
Fig. 1 represents a section on the line I K, almost at right angles
to the sections in Figs. 2 and 3.
The following are the beds represented in Fig. 2 (Section K) :
3. Sbales and sandstooes. > Cretaceous.
4. Black shales. , f
5. Yellow and gray shales. 3
In Fig. 1, the following is the section (Section I) :
1. Sandstones of No. 1, Cretaceous.
2. Yellowish and black shales.
3. Fine hard brownish shales.
g > Shales forming terraces^
As we go south along the west side of the canon of the Gunnison,
we see that the dip, at first, is to the northwest, gradually coming
around to the west. The connection between the Dakota group and the
overlying shales seems to be broken. Opposite station 80, the Bed
Beds (Triassic) are se^n resting on the schists. A little farther south
the Dakota group is washed off, and there are simply remnants of the
red sandstones left. I did not have time to visit this from the west
side, and until this is done, all opinions must, to a certain extent, be
conjectural. As we go farther south we find the granite plateau, before
referred to, shown in Fig. 2, Plate YII,/ to g^ standing between the
Gunnison and the valley of the Uncompahgre. Abutting against this
plateau, at the head of Cedar Creek, and on the branches of Cebolla
Creek, as we have already seen, the Cretaceous sbales are horizontal.
Whether the fold noticed at the northern end of the caiion becomes a
^nfflrrrn
r-r™_
^^^i*«fXitTr S-
^\Jc^..^^,^Xi^^
Library, j
Or I n .rr *
PBALt] GEOLOGY — ^UNCOMPAHGRE RIVER. . 103
fault at the sontherHf I am unable to say. The western side of the
canon will have to be studied before the question can be decided.
Leaving the canon the Gnnnison keeps its westerly course for about
six miles, when it makes some southing to the month of the Uncom-
pahgre, which joins tbe river eight miles below the foot of the caiion.
The trncompahgre is the largest tributary of the Gunnison from the
Bonth. It rises in the Uncompahgre Mountains (Sierra de la Plata of
Oannison*), and has a general course a few degrees west of north. The
range in which it rises is one of the finest in the liocky Mountains.
The geology will be fully treated of in Dr. Endlich's report, the
range being in the southern district. While we were in the valley of
the Uncompahgre, we had a magnificent view of its snowy peaks, which
stand out prominently against the sky. To the west we had a sight of
the Sierra la Sal or Salt Mountains, the peaks being just visible.
Near the head of the Uncompahgre there seem to be some beautiful
open parks. We did not visit them, as our trail led us up Cedar Greek,*
one of the eastern branches of the river. We were but a few miles
above the mouth of Cedar Creek, at the point where the wagon-trail
crosses.
Cedar Creek is probably dry during the greater part of the year. It
rises in a plateau-like divide, opposite a small branch of Cebolla Creek,
a few miles we8tx>f the mouth of the main stream. Its general course is
about northwest. The upper portion of the valley is narrow and^ ravine-
like, the slopes of the hills being covered with scrub-oak, sage, and
cactus, with here and there patches of gras8. This valley continues for
about ten miles, when the creek comes out into the broad valley of tbe
Uncompahgre, which at this point has lines of buttes of light-colored
clayey-beds, the debrisof which forms a soft soil, in which the mules sink
to their fetlocks at every step. All the small creeks, dry for the greater
part of the year, cut deep gullies in this soft soil, which is almost desti-
tute of vegetation. In places there is considerable effioresence of alkali,
and gypsum is found abundantly throughout the valley. The buttes
are found on the eastern side of the valley. They are from two hundred
to four hundred feet high, and form two lines, those nearest the canon
of the Gunnison being the highest. The buttes are not so numerous
in the lower part of the valley, where the general level is but a few feet
above the river-bed. It is more plain-like, without grass, having only a
sparse growth of low sage, interspersed with spots of alkali, giving
the countrv a most desolate aspect Along the river is an alluvial
bottom, with good grass,' the river being bordered with cotton woods,
willows, and low bushes of various kinds. This bottom becomes much
wider as we descend, and is a favorite wintering place for the Ute In*
dians. We found traces of their camps, while their trails run in every
direction. In one place we found a field where corn had been raised, the
stalks of which weie still standing.
On the opposite side of the Uncompahgre the country preserves a
very uniform level for ten or fifteen miles to the west and southwest,
where it seems to rise in a plateau. This level country is terraced, cut
by the branches of the Gunnison and Uncompahgre, which contain
water only in the spring. The terraces are for the greater part desti-
tute of vegetation, being coverd with pebbles, among which are scattered
fragments of chalcedony and agate. They are underlaid with Creta-
ceoos strata, shales in the eastern part, and the sandstones of the Da-
kota group toward the west, as the country rises into the plateau. The
* Pacific Railroad Report, vol. ii, page 55.
104 GEOLOGICAL SURVEY OP THE TERBITORIES.
latter was seen only from a distance, bat it is probably similar to the
country to the west of the Gunnison, near its mouth, the streams prob-
ably cutting through to the Triassicf red sandstones. On the Un-
compahgre the terrace is about one hundred feet high.
On the south side of the Gunnison below the mouth of the Uncom-
pahgre, are three terraces. The first is 100 feet above the level of the
river, the second 150 feet, and the third 200 feet.
Below the junction of the Uncompah^e, the Gunnison keeps a course
a few degrees south of west, until it reaches the mouth of Roubideau's
Creek, nearly five miles below. Here it enters the lower caOon. Above
Boubideau's Greek the valley is very wide, averaging about two miles.
The immediate river-bottom is also broad and overgrown with cotton-
woods and low brush. There are numerous sloughs along the course of
the river, and the fall per mile is very small. The river winds slug-
gishly in curves that sometimes seem to approach circles.
' On the north side are terraces which soon form low hills or battes
reaching almost to the mesa. The edge of the mesa stands boldly out,
like the edge of a fortification-wall. Its slopes are well timbered. The
battes below, extending toward the river, are composed of yellow, gray,
and whitish strata, the weathering of which gives a most curious appear-
ance to the landscape. On the south side, as I have already said, there
are terraces extending southward toward the Uncompahgre Moun-
tains.
The canon which commences at the month of Boubideau's Greek, ex-
tends almost to the mouth of the Gunnison. It is, therefore, about 32
miles in length, in an air-line. By the Ute Indians it is called Unaweep
or Bed Canon,* from the deep-red sandstones that are exposed at va-
rious points along its course. In the caiion the river winds considerably,
and has in places meadows and even groves of cottonwood fringing it-.
It is not very rapid, the fall per mile being about eight feet. Although
in an air-line the caiion is 32 miles long, the length of the river is about
forty-five miles, or perhaps a little more, if we allow for all the smaller
curves. The course of the river at first for ten miles is north 6(P west. It
then flows due north for about three miles, when it turns, taking a coarse
to the northwest, which it keeps generally for nearly fifteen miles, when
it again bends to the west and gradually curves back again to its mouth
in the Grand.
The walls of the canon often rise abruptly from the water's edge in
sheer precipices, while in others there is a narrow strip between the river
and the edge of the bluffs. The latter are betterpreserved on the eastern
side, as the course of the river is nearly at right angles to the dip, which
is approximately to the eastward, really a few degrees north of east.
At the mouth of Boubideau's Creek the walls are only 200 feet high,
while at station GO they are 663 feet high on the eastern side, and much
higher opposite. This probably increases slightly as we go down-stream,
but it can scarcely reach a thousand feet at any point-
At first the river merely cuts through the sandstones and shales of
the Dakota group (Cretaceous No. 1), as shown in a' section of the
bluffs given in another portion of the report.
As we go down, the river gradually cuts through the base of No. 1
into the Jurassic shales and limestones ; and finally, below station 62,
the red sandstones (Triassic f ) appear beneath the shales.
Fig. 3, Plate IX, represents a section across the Gunnison through
station 60 eastward to the mesa terminating the plateau divide. It will
* Vide Pacific Rulroad Report, vol. II, pag^ 57.
4 > •''♦ '
* M
I -
f-.
P1ALE.1 GEOLOGY — LOWER CANON OP GUNNISON KIVEE. 105
•
be seen that there is a gentle slope from the edge of the canon, and that
from the edge of the mesa there is another slope, thus forming a valley
between the two points. This valley is filled with Cretaceous sand-
stones, shales, and marls, which, on the east side, form mesa-like
bottea.
There are five -streams joining the Gunnison from the east in the canon.
The largest is Kahnah Creek. Most of the creeks cut deep caiions as
they join the river. It will be seen, on referring to the illustration
(Fig. 2, Plate IX), that there is a dip at right angles to the stream, and
that this is the greatest at the river, anddecreases as we goawayin either
direction. At the point where the section was made, the dip isouly about
50. Farther north, on the south side of the Grand, the angle is from 15°
to 20°, decreasing as we go westward or south westward to about 6°, and
also decreasing as we go toward the east. There is therefore here a
monoclinal fold, the axis of which has a direction about northwest, the
dip being to northeast. At station 60, the fold is very gentle; but, as
we have seen, to the north it is much steeper, and probably still far-
ther it may become a fault.
Pig. 1, Plate IX, represents a profile of this fold as far north as we
could see it from the mouth of the Gunnison. It will be in one of the
districts during the next season, when it will be thoroughly investi-
gated.
This canon of the Gunnison seems, therefore, to have been outlined by
a fissure in the rocks caused by their folding ; otherwise it would seem
most natural for the river to have cut its way through the soft strata
that lie between the edge of the canon and the basaltic-Capped mesa.
The country to the southwest rises into a broad plateau, beyond which
we could see the peaks of the Sierra la Sal. Ked sandstones seem to
form the basis of this plateau, which is cut into profound canons by the
branches joining the Gunnison on the southwest side. This will be in
the field of explorations next season, and I therefore only refer to it
liere.
The bluffs of the Gunnison as we approach the Grand again fall off,
and do not exceed 150 feet in height. A section at this point will be
found elsewhere, with a description of tbe beds forming it.
CHAPTER IV.
STBATiaBAPHY— ABGH^AN ABBAS OF EAaLE, GBAND, AND GUNNISON
BIYEBS.
As will, perhaps, be evident from the preceding chapters, the greater
portioD of thecoautry comprised in onr district is underlaid with rocks of
Tertiary and Cretaceous age, the older Ibrmations showing only where
there are abrupt folds, and whore the streams have cut through the
more modern beds to them.
The other formations represented are the Jurassic, Triassic (Y), Carbo-
niferous, and Silurian. These will be referred to in subsequent chap-
ters. The present chapter will be devoted to the consideration of the
Archaean rocks, while separate chapters will be given to the sediment-
ary formations, and to the eruptive rocks of the district.
TheArcbaBan areasare limited, and will be considered in the geographi-
cal order followed in the chapters on the general topograph!^ and ge-
ological features of the district.
On account of the rapid and extended character of our explorations,
and also the difficulty of getting at these rocks from their being cut into
deep gorges by the streams, I am unable to present but few lithologi-
cal details. As far as we were able to determine, the rocks are all meta-
morphic, dark micaceous schists prevailing. Until they are studied in
more detail, their exact age must remain undetermined, although the
occurrence of the Potsdam sandstone resting on them near the head of
Eagle Biver, and at various localities in the district of 1873, proves them
to be at lea^t of Pre-Potsdam age. No facts were obtained in regard to
their relations to the metamorpbic series exposed in the Front range.
Eagle River. — The metamorphic rocks through which the upper triba-
taries of Eagle Biver cut their courses form the northern extension of
the Archaean area of the Sawatch range. This area was described in
last year's (1873) report, and therefore I will do little more than refer to
it here. The group of peaks of which the Holy Cross Mountain forms
one of the most prominent, marks the northern end of the great 1^
watch anticlinal. The sedimentary beds curve gradually around the
end of the range, the line of outcrop across which Eagle Biver cuts, on
its way to the Grand being the direct prolongation of the line of out-
crop crossing Frying-Pau Creek (noticed in the report for 1873, page
266).
The upper portion of the Eagle is for the most part in caiion cut in
these rocks. The caiion is one mainly of erosion. As far as the sedi-
mentary beds are concerned it is monocliual. They, however, are not
well shown until we reach the lower part of the canon, which ends a
short distance above the mouth of Boche-Moutonn^e Creek.
This caiion, which has been partially described in a preceding portion
of the report, is about two thousand feet deep, and presents all the pe-
culiarities of gorges cut in gneissic or granitic rocks. The walls are
steep and rugged, the river occupying the entire width of the canon at
the bottom. The trail keeps high up on the hills on the eastern side of
^^fi river.
106
«AUL] GEOLOGY — ABCHiEAN E0CK8 OF GUNNISON AND GRAND. 107
I have already saM that the cauon of Eagle Biver is dae mainly to
erosion. The coarse was probably determined by a line of fracture of
which all evidence has been removed. Inhere is no evidence of glacial
action on Eagle Biver, althongh all.the branches coming from the Sawatch
range show it abandantly, especially Koche-Moutonniie Creek.
The valley of this creek is filled with masses of gneissic rock, beanti-
fally rounded and smoothed by the glacier which once filled its valley.
Grand Biver. — A little more than three miles below the mouth of the
Eagle, the Grand enters a caiion in which it is more than probable
there are ontcrops of metamorphic rocks, probable gneiss and schists.
To verify this opinion the bottom of the canon ough4) to be followed.
The rocks at the entrance of the caiion ^re limestones, which from their
position were supposed to be of Carboniferous age. The course of the
river at this point is a few degrees south of west, while the limestones
have a dip which in general is east. On the north side of the river
it probably changes to south of east, and as we go up the creek that
joins the Grand just above the cafiion it changes more to the north. As
we go down the caSon, therefore, the sedimentary beds ri^e and the
Archaean rocks ought to be seen beneath. This opinion is confirmed by
Mr. Marvine, in whose report this canon will be fully described. He
was on the northern side and had a much better opportunity to study
its features.
He says that on comparing the thickness of the sedimentary rocks
with the depth of the caiion it is evident that the gneiss must show be-
neath. The area, he thinks, is limited, for some five miles down the
canon there is either a fault or an abrupt fold which brings the sedi-
mentary beds once more to the bottom of the canon. With the excep-
tion of this exceedingly limited area, I believe there are no ArchaBan
rocks shown along the course of the Grand, from the mouth of the Eagle
to the month of the Gunnison.
Qunni%(m Biver. — ^The head of the Gunnison Biver is entirely in meta-
morphic rocks, which were described in the reports of last year. Below
the mouth of East Biver, it flows through a belt of Cretaceous rocks,
from which it again enters gneiss and schists, in which it keeps almost
entirely from the month of Ohio Creek to the month of the North Fork.
The only exceptions are where the river flows through broad, meadow-
like valley^, and even here there are schists underlying the river-drift
and alluvium. There are but few of these meadows, and all are above
the Lake Fork of the Gunnison.
This belt of gneiss and schists is narrow for the most part, extending
but a short distance from the edge of the river, except on the lateral
branches where the metamorphic rocks are exposed some distance from
the Gunnison, forming long, tongue like areas. These lateral branches
are generally in canons, and the Gunnison itself cuts a cafion in the
gneiss.
Below the cattle-camp near the mouth of Cochetopa Creek, the pre-
vailing rocks on the sooth side of the Gunnison, for a distance of more
than six miles, are schists and gneiss. Becedmg from the river, vol-
canic rocks will probably appear on top. On the north side, resting on
the gneissic rocks, is a heavy layer of volcanic breccia, underlaid in
places by sandstones, as evidenced by an outcrop not far below the cat-
tle-camp. At station 71, the ArchsBan belt narrows, forming the walls of
a caiion, through which the Gunnison winds with rather a tortuous
course. A section, from station 71 to the river is shown In Fig. 3, Plate
XIY. On the opposite side of the river the rocks are identical. Imme-
diately on the gneiss the sandstones rest, as shown in the illustration. They
108 GEOLOGICAL SURVEY OF THE TEBEIT0RIE8.
are probably of Cretaceous age, belonging to "So. 1 or Dakota gronp.
The reason for this opinion will be given, at length, in a sabseqnentchap-
ter. Farther down the river these sandstones increase in thickness, as
shown in Fig. 1, Plate XIV, while the gneissic area is very narrow.
The presence of the Dakota gronp, resting immediately on the Ar- *
chsBan rocks, wonld seem to prove that in Pre-Oretaceous times this Ar-
chaean area was above sea-level. What its limits were I am unable to
say. It was probably connected with the Sawatch range, a portion of
which, as I mentioned in last year's report, was probably above the sea-
level during Pre-Oretaceons times. There was a period of gradual sub-
sidence. This commenced at least in Pre-Triassic ages; for, as shown in
map B, as we approach Smith's Fork there appear, resting on the gneiss
and underlying the Dakota group, first, beds of Jurassic age, and then
the Bed Beds (Triassic ?).
When the subsequent elevation began it is difficult to say, although
it is altogether likely that it was Post-Cretaceous. It was probably
gradual.
Erosion .subsequently modified the original surface. Then followed
the period* when the breccia and lava was poured out, concealing the
underlying formations. Between Lake Creek and Cebolla Creek, there
are places where the schists and gneiss seem to be capped with trachytic
rock, without any iutervening.layers^ while at lower levels, on some of
the small branches of Cebolla Greek, there are shales probably of Upper
Cretaceous age, abutting immediately against the gneiss and horizontal
in position. . Near the mouth of Cebolla Creek the schists seem to dip to
southeast. Here they are very coarse, with large masses of quartz and
pink feldspar. The mica is silvery (probably Muscovite), The Grand
canon of the Gunnison in reality commences at the mouth of Lake Fork,
although for nearly a mile it is not very deep. Below the mouth of
Cebolla Creek, however, it is between 2,000 and 3,000 feet deep. The
gneissic portion, opposite station 78, shown in Fig. 2, Plate YII, is 2,000
feet deep. The canon extends to the mouth of the Korth Fork.
The ArchsBan area in which this canon is cut is defined in map B, Fig^
2. Plate YII represents a section across it through stations 77 and
78, to Cedar Creek, on the line marked A B, on the map B. Fig. I in
the same plate is a section on the line C D on the same map.
It will be noticed that the metamorphic rocks form a platesCu like mass
between the Gunnison Biver and Cedar Creek. This plateau narrows
to the northwestward and ends in sharp, isolated peaks.
South of station 80 there is, however, as shown on the map, a narrow
ArchaBan belt bordering the river, in which it cuts the deepest (lortion of
its canon. This belt extends to a point below the mouth of Smith's Fork
and forms a bench on each side of the river, as seen in Fig. 1, Plate VII,
at a. It will be seen in map B that the Gunnison Biver keeps on the
eastern side of the plateau, and that on the west (Fig. 2, Plate YII, h to
i), between it and Cedar Creek the strata are horizontal, abutting against
the granitic rock. The age of these beds is probably Upper Cretaceous,
while the sandstones under station 77, at d and e in Fig. 1, Plate YII,
represent the Dakota group (No. 1) or a portion of it.
From the uniformity of level of the plateau it would appear that the
sedimentary beds once extended over it and have been removed by
erosion. In the section Fig. 2, Plate YII, they are shown on both sides
of the river. If they once covered the plateau there must be a line
of faulting along its western edge, for the level of the, Upper Cretaceous
beds shown there is below that of the Dakota group under station
«ALK.l GEOLOGY GUNNISON RIVER. 109
77. Tberefore the western side of the anticlinal fold must change to
a fanlt.
If there is no fault, the force of upheaval must have been greater
on the eastern side of the Archaean ^rea. If this be so it would ac-
'conut for the fact that the Gunnison Eiver keeps on the eastern side,
as seen on the map. We would have to suppose, also, that a portion
of the plateau formed an island in the Cretaceous sea. The western
side of the plateau will have to be followed carefully before the exact
relations can be determined. This I hope to do during next season.
When we were in the Uncompahgre Valley it was late in the season;
there was but little water, and, our supplies being reduced, we had to
make forced marches, so that we were unable to finish the work on the
western side of the canon.*
As already mentioned, the rest of the Archaean area on the Gunnison
is very narrow. It is inaccessible in most places, and I am therefore
obliged to pass by it with merely this reference. The remainder of the
course of the Gunnison is in sedimentary formations, which will be
referred to in their appropriate places.
It will be noticed from the foregoing pages that our district for 1874,
unlike that of the preceding year, is entirely destitute of any metamor-
phie ranges. It is true that the metamorphic rocks on the Eagle Eiver
are a continuation of those in the Sa watch range ; but this portion of
the district forms the boundary, as it were, between the work of the two
years. It was really within the limits of one of the districts for 1873,
but was left unfinished. On the Gunnison and on the Grand, as we have
seen, the metamorphic rocks are ahown in canons where the overlying
formations have been cut through. In no other parts of the district are
there any rocks of Archsean age.
CHAPTER V.
STBATIGSAPHY— PALEOZOIC FORMATIONS.
This chapter will be devoted to the Paleozoic areas of the district
They are as a rule few in number and of small extent. As in the case
of the metamorphic rocks, the Paleozoic formations are found mainly
along the courses of the great arteries of the district, never extending
any great distance from them. They appear there outcropping beneath '
the rocks of Mesozoic age which cover a large part of the region. They
have been identified principally by their position and lithological char-
acters. Although frequent and careful search was made for fossils, it
was generally without success. In Mr. Marvine's district organic remains
were found in more abundance, especially in Carboniferous layers.
I shall take them up consecutively, commencing with the Silurian, and
considering them In the geographical order adopted in the preceding
chapters. On the Gunnison Eiver no sedimentary formations older tban
the Bed Beds (Triassic f ) are seen. At no point in the district was I able
to get the entire thickness of the Paleozoic strata. It is, however, proba-
bly about 4,800 feet.
SILUBIAN AGE.
•
Although no fossils were found by me this year in the strata I shall
refer to this age, still I think their position and lithological characters
warrant such a reference. They rest immediately on the metamorphic
rocks mentioned in the last chapter. We can say definitely that
they are of a Pre-Carboniferous age. The upper portion of the series
may at some future day, when more data are obtained, have to be con-
sidered as Devonian. Fossils of Carboniferous age were found in the lay-
ers resting immediately upon them. There was a much greater de-
velopment in Mr. Marvine's district, and further details will be found in
bis report. In my district, the formation is limited to Eagle Eiver with
possibly a small area on the Grand.
lam unable to make any further division of the formation than to
separate the Potsdam sandstone from the layers above, the base of the
latter being referable to the Calciferous epoch or Quebec group. The
entire thickness of the Silurian layera is about 820 feet
PBIMOBDIAL PEBIOB— POTSDAff t GROUP.
The Potsdam sandstone is widely distributed in the Rocky Mountains,
and preserves its characteristics in widely separated localities. Dr.
Hayden noticed the strata in 1856 or 1857, in the Black Hills of Wyom-
ing, and he and Professor Meek, in a paper read before the Academy of
Natural Sciences, of Philadelphia,* announced the discovery of fossils,
* ProcoediDgs Academy Kataral Sciences^ Philadelphia, March, 1858.
110
Htujtl GEOLOGY — ^POTSDAM GROUP— CANADIAN PERIOD. Ill
identifying them as belonging to the Potsdam gronp. Afterward
Dr. Ha> den fonnd fossils in the same formation in the Big Horn range
in Dakota. In 1869* he also loand, near Colorado City, fossils in layers
just above, that prove the layer in which they were found to belong to
the Calciferoas or to the Quebec group. In the report for 1870, he also
mentions the group.
In 1872 Dr. Hayden and myself recognised the same group in Mon-
tana, near Gallatin City, t The same year Professor Bradley | recog-
nized it in Utah, Idaho, and Wyoming.
ITewberry § speaks of the Potsdam sandstone occurring on the Colo-
rado Biver in Utah. Comstock|| refers to it as occurring in the Wind
Biver Mountains. In all these localities, the genenil characters are
very similar. In Colorado, in 1873, 1 discovered Potsdam sandstone in
various localities, but was unable to discover any organic remains in it,
although just above, I found fossils reierred by Professor Meek to the
Quebec group. Dr. Endlich, in 1873, had outcrops of the group in his
district, while the northern district was without any trace of it.
During the past season I lound on Eagle Biver a series of beds rest-
ing on the gneiss and Schists. From their position and lithological rela-
tions to corresponding beds found by me in 1873, 1 referred the lower
layer to the Potsdam group. The characters of these beds will be given
in the sections a little farther on. Their extent in my district was
limited.
JEagle Biver, — ^The Potsdam group here is represented by a bed of
white quartzite. Near the head of the river it is shown on both sides,
dipping to the. northeast at an angle of 5^ to 10^. It is between 300
and 400 feet in thickness. As we go down the river it caps the ridge
separating the two forks, while the gneissic rocks on the west side of
the western fork are bare, the quartzite which once extended over
them having been eroded away. Still farther along, opposite the canon,
they re-appear in patches, and soon extend from the edge of the canon
in long strips between the branches of the Eagle, toward the Sawatch
range, as shown in Fig. 2, Plate I, representing the Potsdam sandstone
on the gneiss. The inclination is toward the northeast, the angle being
very small. At the point where the section in the illustration is made,
it is shown on both sides, but as we go down the river it gradually dis-
appears on the north, and appears only on the south side, where it con-
tinues to the southward, curving around the end of the Sawatch range.
The inclination increases, and consequently the area occupied by the
Potsdam becomes much narrower, connecting with the belt that extends
across Frying-Pan Creek into the Elk Mountains.
Grand River. — ^The only place on the Grand where the Potsdam group
is likely to be seen is in the canon between the mouth of the Eagle and
the mouth of Bearing Fork. Mr. Marvine's report will treat of this.
Chinnison River, — There is no exposure of this age on the Gunnison
in our district for 1874.
CANADIAN PERIOD— OALCIFEBOnS AND QUEBEC GROUPS.
Although I cannot define the limits of the groups, in ascending from
the top of the Potsdam sandstone^ I have thought it best to give them
* Report United StateA Greological Survey, 1870, page 359.
t Report United States Oeological Sarvey, 187*^, pages 72, 174.
t Report United States Geological Sarvey, 1872. Report of F. H. Bradley.
I Ives's report of Colorado River ; pace 47 of Geological Report.
$ Report on Northwestern Wyoming, by WiUiam A. Jones, page 106.
112
GEOLOGICAL SURVEY OF THE TEEBIT0RIE8.
a separate position here. Calciferous rocks were first recognized- in the
Bocky Mountains in 1869 and 1870. In 1869 Professor Hayden obtained
fossils from near Colorado City, of which Professor Meek says, in the
Report of 1870, page 287 : " So far as these few fossils warrant the ex-
pression of an opinion respecting the age of the rock from which they
were obtmned, I shoald be inclined to place it nearly on a parallel with
the Calciferous division of the Lower Silurian." Prof. F. H. Bradley, in
1872, recognized the Quebec group in Utah and Idaho. Theseriesconsisted
of limestones underlaid by glauconitic sandstones. The limestones were
mostly thin and contained interlaminated shales. The same year Dr.
Hayden discovered beds' of the same age in Montana, near Gallatin City.
There we had layers of limestone also underlaid with glanconitic sand-
stones. In 1873 1 found near Trout Creek, in Bergen Park, Colo., pink
laminated limestones underlaid with glauconitic sandstones. In them I
found fossils referred by Professor Meek to the Quebec group. Anal-
ogous beds had been seen in Glen Eyrie, where Professor H.'iyden,
in 1869, found a few forms that were referred to the same group. I.
obtained a few indistinct fossils there in 1873. On Eagle Biver, above
th6 white quartzite, that has been already treated of as belongiug to
the Potsdam group, we have glauconitic sandstones and qnartzites that
lie below a bluish limestone. No fossils were found here, and I refer
the beds simply on the lithological evidence afi in the following table :
TROUT CEEEK, 1873.
FOUR MILE CREEK, 1873.
EAGLE RIVER, 1873 AND
1874.
Gneiss.
Gneiss.
Gneiss.
•a
1
Yellow sandstone.
White quartzite.
White quarteite.
Pinkish sandstone.
Reddish quartzite.
Dark purplish sandstone.
Qnartzites with shales, glan-
conitic near the base.
Glauconitic sandstone.
Green sandstone.
Quartzite.
a
These beds are glauconitic.
Quartzitio conglomemte^
C3
Blood-red calcareous sandstone
with LingtUepit and Obolus.
Blaeish limestones with layer
of qtiartz'toa near base, con-
taining fragments of Eiurni-
'phahu and Orthit duma-
pleura.
•
k
Pink limestones, containing
Orthis desmopleura, Conoco-
ryphe, A»aphus, Euomphalus,
Lin^ula, BathyurtUf and Para-
doxides or OUtmu.
Light bluish limestone.
It will be observed that the order of the section on Trout Creek is ob-
served in the other sections. Instead of sandstone, resting on the
gneiss, we have quartzite, which in all of the sections is followed by
beds which are glauconitic.
The limestones in the section on Fonr-mile Creek were considerably
metamorphosed, and the fossils found, very indistinct. Still, those rec-
ognized identity the bed as belonging to the same horizon as the lime-
stones in the section made on Trout Creek, which is of Calciferous age.
It may be that in the future the glauconitic beds will have to be de-
muL] GEOLOGY — SILURIAN STRATA. 113
tached from the Calciferons gronp, and considered a part of the Pots-
dam. Not being able to define the boundary between the top of the
series and the next succeeding group, I cannot give the thickness. The
entire thickness of the Silurian will be given in another place.
Eagle River, — ^The Calciferons group is mainly shown on the east side
of Eagle River, until a point below the canon is reached, when it crosses
to the other side. It does not extend up the slopes as the Potsdam
group does, although patches of it may be found scattered over it. It is
entirely conformable to the Potsdam group, and of course follows it
across the country to the southward.
Grand River, — The only locality on Grand River, within our district,
.for 1874, where there is any probability of the group occurring, is in the
canon between Eagle River and Roaring Fork. The canon was not fol-
lowed by ns, and therefore I cannot positively assert that it is shown
there. The reasons for the opinion are given in the preceding chapter
when speaking of the probability of metamorphic rocks appearing there.
Qunniaon River, — The group occurs nowhere on the Gunnison River
from the mouth of Ohio Creek to Grand River.
REMAINDER OF THE SILURIAN.
The remainder of the beds that I have included in the Silurian con-
sist of limestones, which are for the most part magnesian. In one
place on the eastern side of the canon of E^gle River, there is just
above these limestones a bed of trachytic-looking rock, 50 or 60 feet in
thickness. I was unable to trace its extent, but farther north, between
some higher layers, found a bed of similar rock, which was probably
derived from the same source. ^
The following is the section of the Silurian strata, as exposed on Eagle
Biver :
No. 1. — Section of Silurian strata on Eagle River.
Top. Thiolcnefls.
(f> Ft In.
7. Li||fht-blaiBh liinoatoDes on weathered surfaces, white and yeHow. It is
m bands of from three to eight inches thickness, mith a cross frac-
tnre and non-fosAiliferoaSt A great portion of these limestones are
probably magnesian. At the top they are crystalline 219 6
Calciferous Group:
6. Space, in the upper portion of which there is an oat-crop of metamor-
phosed conglomerate, seemingly composed of pieces of white quart-zite
and brown sandstone. The masses are irregularly shaped. The out-
crop is only a few feet in thickness, and the remainder of the space is
! probably filled, with sandntones and quartzites with perhaps a few
shales. The space was so covered that the beds were all coucealed.
The entire thickness is 68 4
5. Milk-white qaartzite, similar to that of No. 1 4 9
4. Space probably filled with sandstones 22 8
3. Grayisn-brown laminated sandat>ones with a greenish coating and mad-
marks ou the surfaces of the laminie 96 6
2. Fine-grained, rather compact, glauconitio sandstone, somewhat lami-
nated, dark brown and greenish-gray... 10 0
Pmimordial Group :
1. Milk-white quartzite 400 0
; Gneiss.
Total thickness Silarian about 819 9
It is probable that a portion of the limestone marked Ko. 6 in the
section above, should be referred to the Trenton, or perhaps to the
l^iagara gronp. It is impossible to say whether No. 7 is all Upper
Siiorian or part Lower.
8 H
1
114 GEOLOGICAL SUB VET OF THE TEBRITOBIES.
The following? table gives the comparative thickoess of the SilariaD
strata an noted ap to the present time in Colorado :
Locality.
ThickneBS of Si-
lorian 10 feet
Gleo Eyrie, on Onmp Creek
^ear ManitoQ, by Mr. Wm. H. Holmes
FroQt Creek, in Bergen Park
In Park range
On Eagle River
North of Grand River, in Mr. Marvine's district
Im Dr. Endlich's district, 1873
113
Mazimnm, 400
150 to 350
350
Maximnm, 500
40 to 80
DEVONIAN age!
Dr. Endlich discovered a series of limestones in his district, in which
there were characteristic Devonian fossils, and Mr. Marvine also obtained
Devonian fossils in his district. While in the field I supposed the
Devonian to be entirely wanting, and I have no positive data by which
to define its limits in my district Still there is the possibility of its
presence; and if so, the limestones jnst above those given in the section
of the Silurian will probably represent the formation. For the present,
and until more reliable data can be obtained than I now have, I will
include them in the section of the lower portion of the Garboniferoas.
They have a total thickness of over 1,000 feet. It is possible that the
lower portion may be of Silurian age. I was unable to get a detailed
section of them, so that all opinions are somewhat conjectui*al.
GARBONyEROUS AGE.
Immediately above the limestones mentioned above, under the head
of Devonian, is a series of strata having a blue fossiliferous limestone at
the base, which is succeeded by sandstones and interlaminated shales
varying from fine-grained and even-textured to coarse and conglomeritic
layers. They are nearly all micaceous, and generally of a greenish-gray
color, although in the lower i)oition they are reil and pink. Some of
the layers contain Carbonaceous material. From the fossils I discovered
in the limestone at the base of these beds, and their lithological identity
with the Carboniferous layers of the Park range as exposed on Foar<
Mile Creek,* 1 have referred the series to the Carboniferous horizon.
It was iiu|)ossible to define the boundary between the Carboniferous
layers and those above, which are probably Permian, as the latter are
comformable and form a continuous series, so I have -arbitrarily chosen
a line to separate them.
The Carboniferous formation was well developed in Mr. Marvine^s dis-
trict, and characteristic fossils were found by him in abundance. To his
report the reader is therefore referred for more detailed information.
£agle River, — On the Eastern bi>inch of Eagle Kiver above the caiion,
and on the branch coming from the Blue liiver range, the formation is
well develoi)ed. Unfortunately we did not have time to follow the
streams, where we might have discovered many points of interest in
regard to these beds.
East of the broad meadow on the eastern branch, above its canon,
.Vir. Holmes, in 1873, found characteristic fossils, Spirijerj ProductuSj
Crinoidsj d;c.
Below the cafion of the Eagle, opposite the month of Roche-Mou*
tenure Creek, the formation is well shown in the blufi's. It, however,
* Section No. 18, page 231, Report U. S. Geol. Survey for ld73. "^
PSALB.) GEOLOGY — SECTION OP CARBONIFEROUS STRATA. 115
MGQ crosses the river, aa the underlying formations do, and extends to
the southward into the district worked over in 1873. Its occurrence
ibere was treated of in the report for that year.
A section of the strata on Eagle Eiver, as shown in the bluffs, will be
pven in the section below. This section is compiled from two sections
I made in 1873. A portion of the beds being exposed at the base of
tbe bluff below the mouth of Roche- Mou ton uie Creek, I had to make a
Mctiou of the lower beds in the bluff above the mouth of the creek
\vhere they were exposed.
No. 2. — Section of Carboniferous strata on Eagle River. %
Top. ThickDess.
Ft. In.
1. PiDk oonglomoritio flandstoneB 37 5
2. Cunglonieritic sandstones and gi*ay phales 92 9
'X Light-gray shales with hard sandstone bands 3 9
4. Blackish micaceous sfaales 3 9
5. Sandstones and interlamluated micaceous scales, some of the sand-
stones conglomeritic 367 2
6. Sandstone conglomerate with pebbles of qnartz from one to two
inches in diameter. This bed is the base of a blnff-like wall, and is
10 feet in thickness. AboTO are beds of shale and coarse sandstone
in alternation. On top is a greenish micaceous sandstone 252 0
7. Coarse, grayish sandstone, with interlaminated shales ; near the top is a
layer of red sandstone, succeeded by a conglomeritic layer 25 1
8. Fine-grained, reddish-brown sandstone 27 4
9. Coarse-grained hard sandstone, spotted with green, general color gray.. 4 0
10. White and greenish-gray conglomerates and shales. First we have
a congloniefitio sandstone, and then green micaceous shales, with
black carbonaceous layers; followed by more conglomeritic layers,
above which is about 15 ft* et of hard sandstone, with interlaminated
soft shales ; then 5 feet of compact gra^ micaceous sandstone. Next
are very soft gteenisU-gray micaceous shales, extending for about 10
feet, followed by from 10 to 12 feet of alternating shales and sand-
stone (some of the latlbr conglomeritic) in beds from 2 to 4 feet in
thickness. Above these are conglomeritic sandstones with shales in
tbe center. The total thickness is about 511 0
11. Coarse white sandstone, with a band of hard fine-grained sandstone near
the top. The micaceous character is marked between the layers 40 0
12. White conglomeritic sandstone 5 0
I'i Red conglomeritic sandstones 38 8
14. Dark-red micaceous shaly sandstones 6 8
15. Brownish-red sandstones, conglomeritic 30 10
IC. Fine-Drained sandstone, generally white, but becoming pink in places,
with two or three layers of gray micaceous shale, each from two to
four inches thickness ■ 4 0
17. Coarse white sandstone, with grains of quartz and some decomposed
feldspar 71 3
18. Soft greenish sandstone in fine layers, with a few hard bunds, each a few
inches in thickness 99 3
li*. Ked sandstone 11 4
^0. Brownish sandstones ^ 99 8
21. Whito granular brown-spotted sandstone 8 0
*^^ Greenish-gray micaceous sandstones, partially conglomeritic - 352 0
ti, A Bpace in which the beds were so much concealed that it was impossi-
ble to make a detailed section ; the upper portion is probably filled
with a prolongation downward of the micaceous shales and sand-
stones, while tde base is limestone. In the Utter I found Avioidopeo-
tettf Pleuropharm, and an Avicula or Bakevellia. The total thickness
of strata as indicated by the space is 408 4
Total thickness of supposed Carboniferous 2, 504 20
Tbe remainder of the section to the beds I included in theDevrnian f is as
ft»ll<»w« :
"U. A laminated tracliytio rock 15 feet.
t &.*? probably fi»«l raaii'ly by lim^tones...... ...... ...-. ) i qoo to 1,500 feet,
26. Blnok llinty limestone, with pifces of pyrite and fragments of > » estimated
S^irifer or 8piriferina j
116 GEOLOGICAL SUfiVEY OF THE TERRITORIES.
llDder tbe head of Devonian, I referred to these beds, and said that they occupied
debatable ground. A portion of tbe npper limestone may have to be referred to tbe
Lower Carboniferons, while tbe lower layers may be of Silurian aj^e, leaving tbe center
to represent the Devonian. Of course, without fossils to prove their age, all opinions
are merely conjectures.
The section given above holds good in detail only for tbe locality in
^hich it was made. The beds ai'e very irregular in their horizontal exten-
sion, some of them thinning oat very rapidly. Thus, for instance, the bed
numbered 17 in the section above, in another place, not more than half
a mile distant, was only three feet in thickness, instead of seventy-one.
One of the illustrations in last year's (1873) report * shows this remark-
al^' well. Not only do they thin ont, but they also change in color
and nature, as we trace them. A bed of red sandstone will gradually
fade into white, while a layer that is Hue-grained in one place will
become conglomeritic as we follow it horizontally. The space contain-
ing beds numbered in the section from 18 to 22, inclusive, in another
place is occupied by light red couglomenite sandstones, with interlam-
inated dark-red' shales. Above the section is a thickness of about
1,300 feet of strata, to which I will refer when I speak of the Permian.
The lower portion might be referred to the Upper Carboniferous, but
as there was nothing to mark the end of the Carbonifei'oas or the begin-
ning, I have arbitrarily separated them.
Below the se<;ond cation of the Eagle are outcrops of gypsiferons
beds, to which 1 will refer under the head of Permian. None of the
limestones or sandstones, referred to above, outcrop until we reach the
Grand below the mouth of the Eagle^
Grand River. — The rocks forming the entrance to tbe canon of tbe
Grand Kiver, thbt extends from a short distance below Eagle Biver to
the mouth of Roaring Fork, are limestones, probably of Lower Carbonif-
erous age. They also form a small cafion on the creek that joins the
Grand at this point. Above, the valley of thg creek widens, and suc-
ceeding the limestones are sandstones forming bluffs, especially on tbe
eastern side. Farther up the creek the gypsiferous series forms the
top of the bluffs.
The following section was made about a mile and a half above the
mouth of the creek :
No. 3. — Section an branch of Orand River.
BaM. ThickneM.
Fl It-
1. Occasional outcrops of coarse gray sandstones, vith interlaminated
greenish shales. The space in which they occur extends from the
base of tbf bluff 150 0
2. Fine black sbaiesi breaking into very fine laniiu» 36 0
3. Coarse conglomeritic white sandstone, in beds of from three to five feet
thickness, with interlamlnated soft greenish shales, in bands from
two to three feet thickness 41 0
4. Very bard, compact, dark, greenish-gray sandstone 32 9
5. Coarse white conglomeritic sandstone 16 ^
6. Hard gray sandstone, in bands of about a foot thickness each, with in-
tenaminated greenish shales 49 1
7. Bluish calcareous sandstone, with their bands of shaly limestone ... 45 0
8. Coarse gray conglomeritic sandstone 2 0
9. Massive yellow sandstones, with bands of fine black shales. These
beds are gypsiferous at the base. They form at^the point where
tbe section the top of the bluff. Thickness about 200 or 300 feet
Total thickness 579-679 feet
*Fig. 15| opposite page 71, Report United States Geological Survey, 1873.
FEAUL] GEOLOGY — ^PERMO-CARBONIFEROUS STRATA. 117
The Strata exposed in the cation of the Grand will be treated of in
Mr. Marvine's report, to which the reader is referred.
Gunnison River, — Nothing was found along the course of the Gunni-
son River that could be referre<i to the Carboniferous.
Id treating of the Carboniferous formation as exposed in our district,
up to this point I have made no division. I have not separated the
Subcarboniferous from the Coal-Measures because I had no reliable
data to guide me in making such a separation. 1 believe, however,
tbat the limestone which lies at the base of the section made on Eagle
River represents the Subcarboniferous, although I cannot say so posi-
tively, and that the sandstone and shales which overlie it conformably
are the representative's of the Coal Measures of the eastern portion of
the United States. As exposed in the bluffs on the eastern side of
Eagle River, these sandstones and shales have black coaly-looking
latere between them, while patches of black carbonaceous material are
of frequent occurrence in the midst of the sandstoues. During their
deposition there must have been, on Eagle Biver at least, low marshy
ground which probably extended around the Sawatch range.
The beds on a creek (Map A) present the same general characters as
those on Eagle River, and belong in all probability to the same horizon,
although without the discovery of organic remains this cannot be posi-
tively asserted. The strata m their horizontal extension, as already
mentioned, change rapidl^^ so that lithological characters are very
uncertain tests of age.
PERMIAN OR PERMO-OARBONIFEROU3.
Under the head of Permian, I will describe the strata that continue
uninterruptedly from the top of the section given under the Carbonif-
erous, to the base of the Red Beds, (Triassicf )
I have called them Permian, from the discovery in the beds on Eagle
Biver of fossils which Professor Lesquereux decided were of Permian
age. On Eagle River, on the Grand and on Roaring Fork the upper
portion of these beds is exposed, and in all these localities the beds are
gypsiferous. They consist of variegated strata, yellow, pink, and
cream-coloi^d shales and limestone, subject to so much change that it
i^as impossible to make any continuous section.
Dr. Hayden found a series of beds in the Black Hills which he re-
ferred to the Permian, as they contained fossils that had been before
found in Kansas and referred to the Permian.
Below the series in Kansas is anotlier set of beds which were also
referred to the Permian by Swallow and Hawn, but which have been
referred by Meek and Hayden* to the Upper CoalMeasures. Between,
however, is a series to which they gave the name of Permo-Carbonif-
erous. Professor Meek says:t ^^This latter distinction, however, it
should be remembered, is, as we have always explained, even in Kansas,
merely an arbitrary one, not founded ui)on any well-defined physical or
paleontological break between these upper beds and the Upper Coal
Measures."
On Eagle River, also, as I have before said, there is no break between
the Carboniferous and the Permian.
In New Mexico, Shumard claims to have found Permian strata in the
Guadalupe Mountains.
* United States Geological Survey, FiDal Report on Nebraska,
tlbid, page 130.
118 GEOLOGICAL SURVEY OP THE TERRITORIES.
Uagle River, — The remainder of the section made iu blnffa on Eagle
Biver near the mouth of lloche Moutonu^e Creek is as follows:
Ifo. 4. — Section of Permian or Permo- Carboniferous strata on Eagle River.
Thleknec«b
Bam. Ft. In.
1. Coarse white oonglomerate • 27 3
2. Greenish-gray micaceons eandstoue shales, with bands of very hard sand-
stone 45 U
3. Very hard irregnlar-stractnred bine limestone, of a brownish color on
weathered surface 10 0
4. Coarse gray sandstone with interlamiuated shales 145 G
5. Massive sandHtones, generally of a gray color, with a greenish tinge. They
are mostly fine-jirained and generally micaceons. Some of the beds are
pebbly, and near the bottom is a band of black shale with carbonaceous
material. This band is from six to eight feet iu thickness. These sand-
stones are exposed in a bluifinthe upper part of which they are cooglom-
critic and darker in color than below 205 10
6. Rather coarse gray sanilstones, in thin beds, fossil iferous, and weathering of
a rusty color 342 4
7. Space probably filled with sandstones and shales reaching to the summit of
the hill back from the bluffs, containing a thickness of about 500 0
Total thickness about 1,276 4
This probably does not represent the entire thickness of the beds, as
I was unable to carry the section up to the base of the Red Beds, and,
farther down Eagle River, where the Bed Beds are present, the strata
immediately beneath are so changed that I could not positively recog-
nize any of the beds of the section made farther up the river.
In bed No, G of the section, in 1873, I found fossils which Professor
Lesqnereux identitied as Catamites sttckoviiy Brgt.jStigmariafucoideSjWi^d
Calamites gigas, Brgt. I qnote his remarks from my report of last year.
Of Calamites suckovii he says: ''This species is perhaiMd more abundant
in the CoalMeasures ; but it ascends to the base of the Permian, where
in Europe, at least, it has been found in plenty." The species was,
however, associated with Calamites gigas^ which Professor Lesquereox
says '* is exclusively Permian and has never as yet been found in the Car-
boniferous Measures.'' Of Stigmaria fuooides he says '*it is a universal
species of the Coal-Measures also ascending, rarely, however, to the base
ef the Permian, I am inclined to consider it as Permian, merely by
the lichological relations to the other specimens, but it is not possible
to decide positively from this."
I think it pi-obable, therefore, that the lower layers in the section given
above may be of Permo-Carboniferous age, as there is but one species
that belongs exclusively to the Permian, while all above should proba-
bly be referred to the Permian.
In contributions to the fossil flora of the western Territories, Part 1 (vol.
vi, Report United States Geological Survey), Professor Lesqnereux says
(page 15) : "In the explorations of Dr. Hayden, 1873, however. Dr. A. C.
Peaie discovered, in strata referred by him either to the Carboniferous or
the Permian, a number of well-preserved branches or stems of Calamiies,
whose identiflcatioii proves for the formation whence they are derived
the same intermixture of characters referable to both the Permian and
Carbonifei'ous.'' "This coincidence in the data furnished by animal
and vegetable paleontology, (referring to some refnarks ffiven upon this
statement^) proves that the end of the Paleozoic times in onr Americau
geology is marked from the Mississippi Biver to the Rocky Mountains
by the Upper Carboniferous, already modified by the first traces of Per-
mian life." Professor Lesquereux, however, says that the Dakota
RALE.] PERMO-CABBONIFEEOUS STRATA OF EAGLE BIYER. 119
group is in immediate superposition to this Upper Carboniferous.
This is probably a mistake, as we will see further on. In going down
Eagle Biver we fiud that these layers, like those of the lower formation,
cross the river and are shown on the western side. From the month of
the Piuey to the head of the second canon of the Eagle, the pru^^ailiug
rocks on the hills bordering the valley on either side, are probably of
Peruiian age. On the eastern side the Bed Beds (Trias t) show above
them on the summits of the hills, which are comparatively low and rounded.
On the western side the Bed Beds do not appear until we reach the head
of the caiiou. The beds here that I have relvrred to the Permian consist
of a series of gypsiferous beds, shales, and sandstones, with probably a
few bands of limestone. I was unable to make any section of them.
Dr. Hayden, in the report for 1873, refers them all to the Carbonifer-
ous, finding species of Prodiictus and Spirifer in the lower part of the
series, and in the upper part a specimen of Orbicula. I have given my
reasons for calling, at least the upper portion, Permo-Carbouiferous, and
Professor Lesquereux has shown that Carboniferous forms are mingled
with Permian in the fossils I collected on Eagle Biver. In Mr. Marvine's
district the gypsiferous beds extended down into the Carboniferous.
Above the canon on the west or south side of the river the area occu-
pied by the gypsiferous series extends some distance back from the edge
of the valley. At the head of the Ciiilou on the west side the dip is south
dOo west. The strata cross the river, conforming to the overlying Triassic
aud Cretaceous hiyers which make the spoon-shaped curve that is repre-
sented in Plate II, and which has already been relerred to. The angle* of
iucliuation at this point is GiP. This, of course, diminishes as the strike
tarns and is parallel to the course of the river.
The following is a general section at this point :
No. 6. — Section of Permo- Carboniferous,
Feet.
1. GypsifeiODS shales and sandstones. The gypsum occnre in great qnantity
aud is rather iuipare. The sandstones are laniianted and f^eueraHy of a
pink or red color. I was unable to gut the exact thickness, but the out-
crop was from 500 to 800
2. Shales, sandstones and limestones, alternating colors, pink, brown, gray,
yellow, white, cream color, aud blackish. Th^ese beds are best shown on the
north side of the river. They incli ue generally abont (30^ . In some plnces
they are inclined past the vertical, especially in the upper portion. The
thickness is about 500
3i. Pink, brown, and gray shaly sandstones with iuterlaminated thin beds of
blue limestone. These beds resemble those I noticed in l':^3 in South Park,
which are given in the report of 1873, in sections 9, 10, aud 11. The thick-
ness on Eagle River is about 200
Total thickness l.;:00
Tlie gypsiferous series is probably tipped up with the overlying beds,
as represented in Fig. 1, Plate I, at e, although they are hidden by the
volcanic overflow. Below the canon they occupy the greater part of the
valley. This area is indicated on the map A. it is difficult here to* re-
duce the strata to any order. Their softness has caused them to yield
readily to eroding influences, and they have weathered into low hills, in
which they are for the most part concealed. There are one or two folds
in them of some extent. These I referred to in the chapter on Eagle
Kiver Valley. Besides, however, there are numerous minor foldings,
which it would require more time than we could give to reduce them to
any system. Mr. Marvitie will probably have some additional notes, as
they extended into his district.
120- GEOLOGICAL SURVEY Oi THE TERRITORIES.
The sections iu Plate III show tbe gypsiferous series below the Bed
Beds at the points marked a. They are probably the same beds I noticed
last year* on Frying-Pan Creek, above shales and sandstones that I
then referred to Carboniferous. I did not know exactly where to put the
gypsifdSrous beds, whether to include them with the Red Beds which were
exposed in the hills above or to place them with the Carboniferous.
In tbe lower caiion of the Eagle, which extends to the month, the
gypsiferous beds are well exposed, dipping from the river on both sides,
leaving the channel in the axis of the anticlinal. Near the mouth of
the river a flow of lava from the hills on the eastern side has forced the
river to the opposite side, and it has scooped out a large jiortion of
these soft beds. The Bed Beds here cap the bluffs on either side.
Grand River, — ^The gypsiferous beds continue from E.igle River to the
Grand, and follow it to within a short distance of the canon, when the
line crosses to the southwest and appears again on a creek, at first odIj
capping the bluffs on the east side, but gradually showing in the bed of
the creek as we ascend. They do not ap])ear again until we cross to
Roaring Fork, where they show beneath the Red Beds of tbe hogbacks
that extend along the western side of the creek, below Rock (^reek.
They are represented at d in Fig. 2, Plate IV. At first the series is seen
only on the western side of Roaring Fork, but as we go down they grad-
ually appear on the eastern side, also extending up a small branch that
comes in from the east. On the western side, at first they have a ter-
race-iike surface. Further down they form bluffs, on the sides of which
they weather into pinnacles and spires of yellow and pink colors. They
continue to the Grand, where the Red Beds appear above them on the
south side, and on both sides of Roaring Fork. Below the month of
Roaring Fork the gypsiferous beds cross the river into Mr. Marvine's dis-
trict. In Fig. 1, Plate IV, they are shown at the point e to/ in the sec-
tion on the north side of the Grand.
Gunnison River, — The gypsiferous series does not show anywhere on
the course of the Gunnison or its tributaries in our district.
* Report of United States Survey for 1873, page 2G6.
CHAPTER VI.
STRATIGRAPHY— MESOZOIO FORMATIONS.
The Mesozoic formations in our district are divided about as folio c^s:
ThickDMs in feet.
Triassio 1,000 to 1,500
Jurnfisic 400 to 900
Cretaceoaa ...4,000 to 4,700
5, 400 to 7, 100
In the Triassic beds the arenaceous element seems to predominate, a
few bands of limestone appearing in the Jar<assic. Sandstones and marls
prevail in the Dakota group. In the rest of the Cretaceous, shales form
the largest portion of the strata, alternating with sandstones and thin
bands of bluish limestone.
The red sandstones of the Trias (?), in the eastern part of the district
have a more laminated structure than was noticed either in the Front
range in 1873, or in the Gunnit^on this year. Gretac^eous strata cover
larger areas than any of the underlying strata, as will be noticed as we
proceed.
TBIASSIO.
Although the red sandstones which are referred to the Triassic form a
well-defined lithological series, and are prominently exposed over the
Becky Mountains and at widely-separated localities, with very little
change, less is, perhaps, definitely known in regard to their age than of
any of the sedimentary formations of the West.
The correctness of the assumption of Triassic age for them depends
entirely upon their position. Up to the present time no fossils have
been found in them. The character of the sandstones is not favorable
to the preservation of organic remains.
They have been referred to the Triassic by Marcou, Newberry, Hay-
den, and others who have studied them in the West.
In the Black Hills and at Red Buttes, on the North Platte, in Wy-
oming Territory, they underlie well-defined Jurassic layers, as deter-
mined by Dr. Hayden. In Golorado, also, they are beneath Jurassic
layers, along the eastern edge of the Front range. Near Pleasant Park,
in 1873, 1 found Garboniferous fossils* in a series of red limestones and
calcareous sandstones. These beds were beneath the red sandstcfnes.
Again, as already mentioned in the preceding chapter, I found fossils of
Permian age below the Red Beds, so that they must be referred either to
tbe Permian or to the Jurassic, leaving an unoccupied gap between.
Therefore, until fossils are found by which their age can be definitely
settled, I think it best to refer them to the Triassic.
Tbe line between the Triassic and the Jurassic is indefinite, and I
* Report United States Oeologicul Survey, lt^73, page 19^.
121
122 GEOLOGICAL SURVEY OP THE TERRITORIES.
have taken the upper or more massive part of the sandstones as the
limit of the Triassic formation, referring all above to the Jurassic.
This arbitrary division was also used by Mr. Marvine last ^ear.
As already mentioueil, these red sandstones vary but little over broad
areas. On the Colorado River they were observed by Newberry.* In
Colorado, last year, we had them in the Front range, in South Park, and
in the Elk Mountains, and they were readily recognized by their litho-
logical characters. Their general massiveness was a prominent charac-
teristic.
Eagle River, — Near the head of Eagle Elver the Bed Beds do not ap-
pear close to the river, although they are doubtless exposed between the
Blue River range and Eagle River. Below the Piney they outcrop in
the hills bordering the valley on the east. The strike here is parallel,
or nearly so, with the course of the river. At the head of the second
canon, however, the line of outcrop crosses the river almost at right
angles to its course, first making a spoon-like curve shown in the illus-
tration in Plate II. On the south side of the river it curves to the west-
ward, and then gradually to the north, crossing the river again at the
foot of the caOon, as shown on the map, (A,) and extending up into Mr.
Marvine's district. Opposite the canon, that is, south of it, this curve
forms the northern side of an anticlinal fold or break, which is shown in
Fig. 1, Plate I, caused by the protrusion of the trachytic mass shown in
the illustration.
A section of the Red Beds, as exposed near the Eagle River, on the
south side, is given below.
No. 6. — Section of Triaasic on Eagle River at second caiion.
Base. ThicknctBb
feet
1. Red BandstODes, somewhat laminated 70
2. Purplish sandstones 15
3. Red and brown laminated sandstones, some of the layers being seemingly
calcareous 193
4. Coarse white sandstone 5
5. Red sandstones, more massive than the lower layers, althongh there is some
lamination 375
6. Pink quartzitic sandstone ) ^aq
7. Red sandstones somewhat laminated 5
8. Massive light-colored quartzitic sandstone 10 to 20
Total thickness :-. 978
It will be noticed in this section that there is considerable lamination
in the red sandstones. Farther westward this lamination is not so
decided.
Below the cafion, in the hills that rise back of the low gypsiferons
bills, the Red Beds form the surface, covering a large area, extending
across to Frying Pan Greek. They form broad-topped ridges, in which
the general dip is toward the north, the inclination being slight. As
we approach the valley of the Eagle, however, it increases and we
have several folds, as pointed out in the chapter on Eagle River Valley.
On station No. 8, the red sandstones dip a few degrees east of north.
On station No. 9, they dip North 35© West, angle 30O-^o.
I have already spoken of the probability of there being here a
synclinal fold, of which the eastern half has been removed. This fold
is indicated in the illustration Fig. 1, Plate III, by the dotted lines. Below
the valley, the river flows through a canon-like valley in the axis of an
* Ives^s Colorado Exploring Expedition, Geological Report.
PiALB.) GEOLOGY — TRIASSIC STRATA — GRAND RIVER, 6lC. 123
aDticlinal, which is sbown at a ainFig.l, Plate III, the Red Beds forming
the top of the bluffs od either side of the river, as shown in the figure.
Grand River, — From the mouth of Eagle liiver the Bed I^edscap the
blufi" for some distance, when the line of outcrop crosses to the south-
ward and afterward to the east, joining the line continuing westward
from h creek (map A), thus forming an isolated area of red sandstones.
Between the Grand and Koariug Fork, there is another patch of Red
Beds, which is partially concealed by an overflow of lava. On the west
side of Roaring Fork we have the Red Beds showing in the hog backs.
Their thickness here is about 1,500 feet. They dip south 75^ west, at
an angle of 30^, below station 14. The upper part of the series here has
layers of pink conglomerate sandstone.
As we go down Roaring Fork the strike curves to the westward, and
the Red Beds disappear beneath a layer of volcanic rock which covers
the hills here. They reappear on Grand Riverou the south side, a short
distance below the mouth of Roaring Fork, forming high bluffs, that rise
600 or COO feet above the level of the river. The Grand then gradually
cuts into thered sandstones, following the strike, which is about north 60'^
west for nearly four miles in an air-line, forming the base of the hog-
backs that here extend along the southern side of the Grand. The
river then cuts across the strata, flowing out into higherand softer beds,
while the Red Beds cross into Mr. Marvine's district. From this point
to the mouth of the Gunnison there are uo exx)osures of the Triassic
sandstones.
Gunnuton iJtver.— The Triassic sandstones do not- appear on the Gun-
nison River until the lower half of the Grand Gaiion is reached. They
seem to increase gradually in thickness, although the total thickness
attained in the canon is not very great. They rest immediately on the
granite shelf forming the edge of the canon below station No. 80. The
ana occupied by them along this caiion is indicated on map B. At
station 80^ the anticlinal axis occupied by the river is very evident.
It is shown in Fig. 1, Plate VII, at a. Leaving the caiion the river cuts
across the northern end of the anticlinal, and, turning to west, flows
out into the soft shalesof Cretaceous age. In the second or lower caiion
the river cuts down through the Dakota group and the Jurassic layers,
and partially into the Red Beds.
The top or' the series here is a pink sandstone, from 30 to 40 feet in
thickness. The thickness of the red sandstones varies. Below station
60, where the pink sandstones were measured, the thickness exposed is
about 150 feet- They are massive and present all the characteristics
that the Red Beds east of the mountains do. They dip approximately to
the eastward, the angle decreasing as we leave the river and increasing
to the west. The river winds through the canon in large curves that
almost meet each other. Whenever the curve is to the westward the
led sandstones are cut into most deeply, and when the curve is in the
opposite direction the Red Beds, if exposed at all, are only cut into
slightly. This causes the areas of Triassic age to appear in patches
along the course of the river. All the streams joining the Gunnison
from the west cut profoundly into the strata, and near their sources,
niay have outcrops of Pre-Triassic layers along their courses. I have
already referred to the fact that the Gunnison River at this point fol-
lows a rift or break, which was probably caused by a monoclinal fold. .
Two sections sicross this are shown in Figs. 1 and 2, in Plato IX. At
first the fold as shown in Fig. 1 is not very marked. It gradually
increases, however, and below the mouth of the Gunnison is as repre-
124 GEOLOGICAL SURVEY OF THE TERRITORIES.
sen ted in Fig. 2. Farther on this fold probably becomes a faalt. In the
two figures just referred to, the red sandstones are represented at a.
To the west and southwest of the Gunnison the red sandstones seem
to prevail extensively, and probably from the top of the plateau which,
as seen from the G.unnison, extends in this direction. The Indians give
the lower canon of the Guunison the name of Unaweep or Red Earth,
evidently on account of the exposures of Ked Beds along the edge of the
river.
JURASSIC.
Immediately abovethe Red Beds, between them and the Dakota group,
is a t^eries of sandstones, marls, and limestones which I have referred to
the Jurassic, although I was unable to find any lossils at any point
where they were exposed in our district of 1874.
They correspond lithologically and stratigraphically to the strata that
in 1873 I referred to that horizon. The reasons for so doing were stated
in the report for 1873, and I will not take up the space here with the
repetition of them. They are generally in thin beds, the shaly element
predominating. Their softness has rendered them readily amenable to
eroding influences, so that they are generally covered with debris^ and
it is difficult to make complete sections of tbe formation.
The Jurassic formation is widely spread in the Rocky Mountains, its
distribution being identical with that of the Dakota group and the un-
derlying Red Beds. Hayden, Newbery, Comstock, and others have
recognized it in various portions of the West. Marcou* also claims to
have discovered it in New Mexico and other parts of the West, but, as I
shall subsequently point out, the layers referred by him to this horizon
are probably of Cretaceous age, while those that are Jurassic he refers
to the upper part of the Triassic.
Dr. Hay dent, speaking of the formation, says: "At both of these
localities {near the Wind River Valley and Big Ilorn Mountains)^ at the
Black Hills and ^t the Red Butte on the North Platte, as well as at
the other localities already mentioned in Utah (near Uintah and Weber
Bivers)y the rocks containing these Jurassic fossils consist of a series of
grayish, ash-colored and red argillo-calcareous, more or less gritty
strata, with beds of soft dark-brown and reddish sandstones. Tbese
Ibeds preserve a remarkable uniformity of character taken as a group,
wherever they have been seen, and need never be confounded with the
Cretaceous or Tertiary rocks so widely distributed over the Northwest-
ern Territories, even where no fossils are to be found."
In Colorado, Dr. Qayden, Mr. Marvine, Dr. Endlich, and myself found
the Jurassic layers presenting the same general characters that they do
north of the Union Pacific Railroad. Along the eastern edge of the
mountains in Colorado, the greatest thickness measured was 870 feet.
Eagle River. — On the south side of the river no strata of Jurassic
age appear until we reach the head of the second cation, when it crosses
from Mr. Marviue's district conformable with the overlying Cretaceous^
and underlying Triassic.
The following is a section made on the south side of the river at the
point where the section previously given of the Triassic sandstones
was made.
•
*Geo1ogy of North America, by Jules MarcoD.
tGeoIof^ical Report of Exploration of tbe Yellowstone and Missouri Rivers. F.V*
Hayden, under Capt. W. F. Raynolds, 185*J-*60.
mLE.1 QEOLOGT— SECTIONS OP JDRASSIC^EAGLE BIVEB, &C. 125
No. 7. — 8ectwn of JuraHtdc^ head of second canouj Eagle Biver^ south side.
Top. ThicluieM in feet
1. Space probably filled with sandstones and marls, aboat 500
2. Laminated sandstones and blue limestone ? joq
X Li^bt-yt'llowish brown sandstone >
4. Blue limestone 50
5. Gray Hbaly sandstones with interlaminated marls and thin bands of bine lime-
stone 200
Base ~^-~~
Total about '. 940
A portion of these bids may be Cretaceoas.
No>^here along the course^of the Eagle, nor at any point in the dis-
trict, does the Jurassic formation occnpy any extensive area. It occurs
only as a narrow belt outcropping beneath the Dakota group. It is,
therefore, shown principally along the courses of the streams.
The line of outcrop on which the section given above was made con-
tinues conformable with the Cretaceous and Triassic strata, following
the curve indicated on the map, and crosses to the north side of the
Eagle at the lower end of the cation.
Around the almost circular area of Cretaceous rocks south of the
Eagle, represented on the map, there is, in all probability, a narrow belt
of Jurassic, although I cannot be positive, as I have not followed it
around, and judge so only from my observations from stations 6 and 8.
With this exception, I believe there are no Jurassic strata exposed be-
tween the Eagle and Frying-Pan Creek. Ih the low, rounded hills
which occupy the greater portion of this space, all the beds above the
Triassic sandstones have been removed.
Orand River, — From the mouth of the Eagle to the tnouth of Roaring
Fork there are no exposures of Jurassic age close to the Grand. The
Bed Beds here form the top of the strati&ed rocks and are covered with
a volcaiuic layer. There may be an occasional outcrop between the
bead of a creek of Grand Bi ver and Roaring Fork. If so, they mnst be
very limited in extent. At the head of Mesa Creek, a branch of Boar-
iog Fork, there is probably a narrow belt dipping to the south or south-
east.
In the hog-backs, on the west side of Soaring Fork, the Jurassic
strata are seen following the line of the overlying and underlying strata,
disappearing beneath the volcanic rock capping the hills, and re-appear-
ing on the Grand below tbe mouth of Boaring Fork, Anally crossing
the Grand, ai' J extending to the northwest, forming a portion of the
hog-back range, that dies away in the plateau. Between this point and
the mouth of the Gunnison there are no other exposures of Jurassic
age along the course of the Grand.
No. 8. — Section ofJurassiCy west side of Boaring Fork, beloic stcction No. 14.
Base. ThiokneM in feet
1. Coarse gray sandstone 20 to 30
^. Space probably filled with sandstones and shales 20
3. Fine-textnred light-yellowish sandstones 15
4. Space probably filled with sandstones, marls, and shales, and perhaps some
limestones 165
5. Light-colored fine-grained siliceons sandstone 30
6. Sou shaly sandstone, probably slightly argillaceons 12'
7. Blue limestone 8
8. Gray sandsto nes, becoming green ish near tbe npper part 125
9. Dark-brownish gray sandstone, becoming lighter as we ascend 15
10 Brownish sandstone with interlaminated black shales 20
Top.
Total aboat 440
126 GEOLOGICAL gURVEY OP THE TERRITORIES.
Jast above the bed marked Ko. 10 in the Bection ia a massive sand-
stone, from 60 to 70 feet thick, which forms the summit of a prominent
hog-back, beyond which the beds are concealed. I have taken this bed
as the lower portion of the Dakota gronp. It is possible that on further
investigation the layers marked 8, 9,. and 10 may have to be incladed
in the Dakota group. This would give a total thickness for the Juras-
sic at this point 280 feet instead of 440 feet.
Below tbe first layer in the section is a coarse pink sandstone, which
at some points is a conglomerate. It rests immediately on the red
sandstones, and I have taken it as the top of the Triassic. Of course,
without the evidence of fossils, the lines separating the Jurassic from
the Cretaceous and the Triassic must be necessarily, somewhat indefi-
nite. The lines I have taken are therefore arbitrary and liable to be
changed when more complete data are obtained
In the section given above, and in that made on Eagle River, it will
be noticed that the arenaceous element seems to predominate. The
beds were so much concealed that it was impossible to make a more
detailed section. The extension of the hog-backs up Rock Creek into
tbe Elk Mountains will be tresited of in the reports of Dr. Hay den and
Mr. W. U. Holmes.
Gunnison River, — The Jurassic appears on the Gunnison first in the
Grand Canon, resting immediately on the schists, and gradually becom-
ing thicker as we go down the river, until the Red Beds appear between
it and the schists. The Jurassic is also exposed on Smith's Fork,
extending some distance from the mouth up the stream.
The area occupied by the formation, in connection with the Red Beds,
is shown on map B.
I was unable to make any section in the course of the caiion, but, as
seen from station No. 80, it appears to consist of variegated yellow,
white, pinkr and gray beds, probably sandstones, shales, and marls. On
the eastern side of the caiion these beds have a much greater extension
than on the west. The entire thickness is X)robably about the same as
in the lower caiion, as shown in the section to be given farther on.
On Smith's Fork, the variegated appearance of the Jurassic strata is
also seen. In the sections made on Eagle River and Roaring Fork, this
is wanting. I shall refer to this fact again. In the lower caiion the
Gunnison very soon cuts through the Dakota group, which, at the head
of the caiion,* forms the bluffs on either side, and reaches the soft
Jurassic layers beneath.
At first they are exposed in isolated patches similar to the outcrops
of the Red Beds lower down, varying according to the curves of the
river. When the Red Beds are reached, however, the Jurassic is shown
on both sides of the stream.
No. 9. — Section of Jurassic in the loicer carton of Ounnison River near
Station (iO.
Base. Thiokoeaa.
Ft, In.
1. Soft greenlBh and parpliah argillaceous BandstoDes about 20 0
2. Space tilled with gray laminated liiuestoues and iaterlamioated soft gjp-
siferous shales ". BO to 90 0
3. Compact white siliceous pandstuoe 8 9
4. Soft argillaceons and arenaceons shales, with bands of bard sandstone
from 0 inches to a foot in tbickness. The sbcles are covered with an
efflorescence of alkali, in which there is salt, as revealed in tasting it.. . 30 0
5. Compact white sillceons sandstone, like that marked No. 3 6 10
6. Dnll bluish'frray limrstone, in layers of about a foot thickuess, having
shaly arenaceons and argillaceous beds between. Near tbe top arc soft
greenish and pink shales. All the beds are more or less gypaiferoas.. 35 0
KA1E.J GEOLOGY — ^JURASSIC STRATA IN ARIZONA. 127
«
ThiclmeM.
Ft. In.
7. Tellow siliceoTis sandstone «^ 2 0
8. Soft green sandstones and argillaceons shales
9. Space covered where the section was made, but as seen from a distance
lower down the river filled with beds similar to those of No. 8. ...... .40 to 50 0
Top.
Total thickness about 248 7
Above layer I^o. 9 is a massive siliceous sandstone, which I have taken
as the base of the Dakota group, for reasons that will be given when I
describe the Dakota group at this locality. Below the section are pink
Bandstoues, resting on the red sandstones, referred to the Triassic.
The colors of these layers gives a unique and striking appearance to
the canon-walls. Farther south and west this variegated appearance
seems to be more marked.
In the Painted Desert in Arizona, Newberry* gives the following sec-
tion of the beds :
Variegated inarU,
Thiokneaa.
Ft. In.
1. Light orange marl 15 0
2. Green and purple magnesian limestone^ containing worm-like concretions
of calcareous spar 5 0
3. Pinkitth-purple marl S2 0
4. Brown shelly sandstone 0 8
5. Purple marl with silicified wood 16 0
6. Purplish green cherty magnesian limestone^ in seyeral layers, alternat-
ing with bands of marl 8 0
7. Purple and cream colored marls 30 0
8. Greenish magnesian limestone in thin layers, with bands of marl 12 0
9. Yellow, red, and purple marls 40 0
10. Green limestone, similar to No. 8 3 0
11. Red, purple, pink, green, lilac, brown, and blue marls with silicified
wood A 350 0
Marconf refers these beds to the Trias, regarding them the equivalent
of the J^arnea Irisies of France and of the Keiiper of Germany. He
says, "The third division or upper group of the Trias is subdivided
agiHo into two parts. The lower is formed of thick beds of whitish-
gray sandstone, often rose-colored and even red ; and the u|>per con-
sists of beds of sandy calcareous clay, of very brilliant colors, violet,
retl, yellow, and white — in a word of variegated marls. This upper por-
tion presents a striking resemblance, as to the rocks, with the Marnes
Irism of France, or the variegated marls of Euro|>e."
Above the section (No. 9) I made ou the Gunnison is a bed of massive
sandstone succeeded by shaly and marly beds, in the upper portion of
vhich is a lignitic layer.
Above the variegated marls of the section given above, Newberry J
fonnd a bed of lignite which he considered to be of Jurassic age.
Whether this is identical with the lignite in sections Nos. 12, 13, and 14,
I cannot positively determine, but I think it improbable, as the beds
below do not seem to be ideuticaL If they are identical, I place the
lower limit of the Dakota group lower than he did. The reasons for
so doing will be stated hereafter. Newberry, in .his sections of what
he considers the base of the Lo>yer Cretaceous, also finds a lignitic bed,
which is probably the one I have included.
Newberry§, in speaking of the lignite, says : '* The sandstone shales
and limestones lying above also include many beds of lignite closely
*Ives's Colorado £xpk>ring Expedition, Geological Report, page 79.
t Geology of North America, page 13.
t Ives's Colorado Exploring Expedition, Geological Report, page 81.
i Ives's Colorado Exploring Exptdition, Geological Report, page 63.
128 GEOLOGICAL SURVEY OP THE TERRITORIES,
resembling this, and on litbological grounds woald be appropriately
grouped with it. In fact they have been considered Jurassic, and the
only Jurassic rocks in this region, by the geologist who claims to have
discovered the representatives of this formation in New Mexico. Unfor-
tunately, however, for that classification, immediately over the thin
stratum of yellow sandstone which overlies the coal are beds of clay-
shale with bands of limestone in which are unmistakable Cretaceous
fossils. It is, therefore, evident that the Jurassic formation cannot be
extended in this direction, and there is no alternative left but to con-
sider the coal-seam, if Jurassic, the sole representative of the Jurassic
series, or to combine with it some portion of the underlying variegated
marls, which, for this purpose, must be abstracted from the Trias of
Mr. Marcou."
CRETACEOUS.
It is, perhaps, impossible at present to subdivide the Cretaceoas
formation, as seen west of the continental divide, in the same manner
as has been done east of the mountains.
For the sake of convenience in description, it may be best to consider
it as divided into three groups, Lower, Middle, and Upper Cretaceous,
as follows :
inieet
Lower Cretaceous — Dakota gronp (No. 1) 500-700
( Fort BeDton group (No. 2), )
Middle Cretaceous — < Niotrara division (No. 3), > 2,000
( Fort Pierre group (No. 4), )
f Fox Hill beds (No. 5). ^
Upper Cretaceous-J ^ ««^»f « «^ f ^^7, f*°<l«*«°/«;^^»^VV^^^^
xj^^ro,. xy^«i.»^«>vuo X part are lignitic. On Autbracite Creek this f •*»*'^ »
t lignite is changed into anthracite coal . . . _ . J
Total 4,000-4,700
This table represents the estimated thicknesses as developed in oar
district.
LOVTEB CRETACEOUS.
Dakota group — Formation No. 1.
Immediately above the group of shales last described, under the head
of Jurassic and conformable to it, is a series of beds in which rather mas-
sive siliceous sandstones predominate. It is ))ersistent throughout the
Bocky Mountains, preserving it-s litbological characters very constantly
over widely-separated areas.
The group forms a convenient horizon for reference, being more
strongly marked, perhaps, than any other in the sedimentary series. Its
age is well established, and I will therefore not take the space here to
repeat the evidence. The discussion in full will be found in Professor
Lesquereux's " Cretaceous Flora of the West." •
The evidence as to its identity in Colorado is as follows :
During the explorations of 1873, near the exit of the South Platte
Biver from the mountains, I found fragments of a Proteoide8j\ of which
■ Professor Lesquereux, writing me, said : ** It is very near Froteoides
acuta (Beer.), if not a small form of the same."
As yet no leaf of this genus has been found higher than the
* Report of United States Geological Survey, vol. vi ; Cretaceoas Flora, by Leo
Lesqnercnz.
t See Report of United States Geological Survey for 1873, page 196.
»ALK.J GEOLOGY DAKOTA GROUP — ^EAGLE RIVER. 129
Dakota group. In tbe same series I also found, near Glen Eyrie, a few
miles from Colorado City, specimens of a liugula too indistinct for spe-
cific identification. In the Elk Mountains namerous impressions of
dicotyledonous leaves were noticed, most of them fjagmentary and in-
distinct.
On the Gunnison Biver during the past season (1874) I found a frag-
ment of a sassairas-leaf like 8. mirabilej near station 60, and in the
blnffs near the mouth of the Gunnison I obtained a Cretaceous IScaphite.
Id various parts of the Elk Mountains Mr. Holmes found impressions
of a Salix.
Professor S'ewberry* recognissed tbe group in New Mexico. I shall
hereafter refer to the identity of his sections with those made by me
ou the Gunnison.
Speaking of the rocks as exposed in Kew Mexico, be says : *' The
paleontological evidence of tbe age of these rocks is quite conclusive
and of unusual value, as it fixes tbe place in tbe geological scale, of a
well-marked formation in New Mexico, and one which has been the sub-
ject of considerable discussion. In the second member of the Cretace-
ous portion of the section, counting from tbe base upward, are con-
tained fossils which are characteristic of the Cretaceous formation in
Texas and Nebraska. These are Inoceramus crispii and Oryphwa pitcherij
well known Cretaceous fossils, common in Texas and the Indian Terri-
tory, and, in greater numbers, specimens of an ammonite {A.ptricarina-
tu»)j higbly characteristic of Nos. 1 and 2 of Meek and Haydeu's section
of the Cretaceous rocks on the Upper Missouri. There is no doubt of
tbe parallelism of the group of sandstones with those of the base of
Meek and Hayden's Cretaceous section."
Tbe litbological characters will be shown in the various sections
given, as I consider the formation according to its geographical distri-
bation in our district.
Eagle Biver, — Until we reach tbe bead of the second canon there are
no outcrops of Cretaceous age on tbe south side of Eagle Uiver. Here,
however, the sandstones of tbe Dakota group cross from the north and
form a semicircular ridge, crossing to the north side again at the lower
end of the cafion. In Plate 11 tbe group on tbe north side at the bead
of tbe canon is shown at a a.
The semicircular line of outcrop is shown on map A. Stations 6 and
7 were located on its edge. The dip of the strata on station 6 was North
50 East, and on station 7 North 85^ East, the angle of inclination about
2(P. In this basin, included between the ridge and the river, tbe overlying
strata have almost entirely been removed, the upper part of the group
forming the greater part of tbe floor of the depression or semiquaqua-
versal. A section through the center of this basin is shown in Fig. 1,
Plate 1, from the point a to the Eagle Iliver. 1 was unable to get a
iteetion here, so that I cannot say bow thick it is. On station 6 the
rock is a coarse white siliceous sandstone. Where it is in contact with
the volcanic rock, as seen in the section and on tbe map, it is meta-
morphosed.
Below station No. 7 there is tbe following section, from below up :
1. Gray sandstone, greenish coating on the surfaces of the lamin®.
2. Hard greenish mottled limestone.
3. Greenish gray sandstone.
4. Blue limestone.
5. Sandstones forming the station.
* Ives's Colorado Exploring Expedition, Geological Report, page 85.
9 H
130 GEOLOGICAL SURVEY OP THE TERRITORIES.
The lower portion of this section is probably Jnrassic.
The area of (^retaceoas represented on the map lying between the
semicircular ridge and g creek is probably almost entirely of the sand-
stones of the Dakota group. There may be some of the' layers of No.
2 and No. 3 in places, as shown in Fig. 1, Plate I. There are no other
outcrops of No. 1 on Eaigle Kiver or its tributaries within the limits of
our district.
Grand River. — Between the Grand and Roaring Fork, at the head of
Mesa Greek, there are, judging from the view we had from station No. 11,
outcrops of the Dakota group dipping to the southwest. It also oat-
crops beneath the mesa between this creek and Frying-Pan Greek, near
the base, on the south side. Between the Grand and Boating Fork
there may be a few patches of Gretaceous, but, if so, I think they are of
higher beds than the Dakota group. On the west side of Roaring Fork
it forms the summit of the prominent hog-back ridge. On station 14 it
is a massive light grayish siliceous sandstone, the outcrop of which
measures 63 feet. If the beds marked 8, 9, and 10, in the section of the
Jurassic (section No. 8) made here, are included, the following would be
the section of the Dakota group at this point.
No. 10, — Section an Station No. 14,
Top. TbiokneM in feet
1. MnsBive grayish white siliceoiis sandstone 63
2. Brown sandstone, with fine black shales ^
3. Dark brownish-gray sandstone, becoming light-colored near the top 15
4. Light greenish sandstone 1>^
Base. —
Total,abont 203
The character of these beds, I think, warrants their being considered
Cretaceous rather than Jurassic. The bbick shales in No. 2 probably
occupy the same horizon that in the other places is filled with the ligiiitic
beds. If they are not considered Cretaceous we have only a thicknesa
of 63 feet for the Dakota group. Above the layer marked No. 1 the
beds have been eroded and covered with the dSbria^ leaving a valley
between the hog back and the hills to the west. On the Grand, below
the mouth of I^aring Fork, the Dakota group comes out from beneath
the volcanic rock of station 16. At station 14 the strike of the hog-
backs is north 15° west, and the angle of dip 3Uo. Station 17 was ou the
sandstones of the DakoUi group. The inclination here is 35^. This
seems to increase to 50° or OO^ to the westward. The strike is north 15P
to 80O west. The hog backs extend about seven miles beyond station
17, when they cross the river into Mr. Marvine's district, and the Grand,
from that point to the mouth of the Gunnison, flows through beds of
higher horizons, not reaching the No. 1 until the river is joined by the
Gunnison. Here it outcrops in the bluff's. I will reserve the description
to the section devoted to the Gunnison.
Gunnison River. — At several points bordering the meadow-like expan-
sions of the valley of the Gunnison below the mouth of Cochetopa Creek,
there are indistinct outcrops of sandstones that probably represent a
portion of the Dakota group. As we proceed down the river these oat-
crops becomemore distinct, and below station 73, besides the No. 1, shales
of No. 2 are represented, shown at c in Fig. 1, PlateXIV. The Cretaceous
rocks seem to have been subjecticd to considerable erosion, preceding the
lava flow that has covered them. This is shown by the change in the
strata shown in the figures in Plate XIV, which are sections on the north
mLK] GEOLOGY — DAKOTA GROUP — GUNNISON RIVER. 131
side of theGiiDDison at various points between the month of Goehetopa
Creek and the mouth of Lake Fork.
The drainage had probably then the same general direction it has at
present. In Fig. 2, Plate VII, beneath station 77, at the point d, we have
on top of the Dakota gronp a few shales. Farther north, at station 79,
there is greater thickness, reaching in all probability as high as No. 4.
The wearing down was probably from north toward the south, which is
the general direction of the streams at present.
The following section was made from the point a to 5, in Fig. I, Plate
XIV.
No. 11. — Section of No, 1 Cretaceous^ beneath station 73 north side of Gun-
nison River.
Base. ThiokoesB in feet
1. Dark micaceotis gneiss
0-2. SiliceooB saudstoney general color yellowish, becoming pink and white in
places. The lower portion is somewhat concealed in beds that are raussive. 43
3. Siliceous sandstones like those of No. 2, general color pink. These sandstones
are not so massive as those of No. 2. They are somewhat laminated 58
4. Yellow sandstones in bands of two and three feet thickness, 32
5. Sandstones and interlaaiinated shales. The general color of the sandstones is
yellowish ; some of the layers have greenish pebbles. Tbe shales near the top
are greenish • 79
6. Laminated brownish-gray sandstones in bands from a foot to eighteen inches
in thickness. There are greenish-gray interlaminated bhales. Some of the
sandstones are probably urgillaccons and weather into rounded bowlder-like
masses 6
7. Spacefilled with baudsof sandstone and soft argillaceous shales and limestones.
In the lower part there is a nodular limestone with pebbles of red jasper.
Tbe upper parts of the sandstones are faintly tinged with purple 82
8. Greenish and yellowish indurated argillaceous sandstones and shales, resem-
bling the beds of No. 7 52
9. Soft yellow and white laminated sandstones 10
10. Soft pinkish laminated sandstones 14
11. White argillaceous sandstones and shales; some of the beds are indurated and
break with a conohoidal fracture. The sandstones weather with rounded
corners, forming bowlder-like masses as in the case of No. 6 54
12. Massive yellow siHceous sandstones, about 100
Top.
Total, about 536
These sandstones and shales are exposed on both sides of the river
beneath the breccia, and also for soine distance up the lateral branches.
North of the Grand Canon the gently-sloping surface between the
Gunnison and Smith's Fork is underlaid by the Dakota group, which
forms a bluff-like edge above the granitic shelf bordering the canon.
Tbe slope is about lour degrees in a direction a little east of north.
Smith's Fork cuts through the No. 1 almost parallel to its strike. The
beds here have the same general character that was noticed in the sec-
tion given above. In some places on Smith's Fork I noticed black coaly-
looking shales, and in some of the laminated sandstones were ripple and
mud marks.
Near the head of the south branch of Smith's Fork the gentle slope
of the Dakota group is broken and the stream flows through a small
canon caused by the breaking. Tnis canon is marked a a on map B.
It is only about two miles long. On the west side the dip of the
strata is 5<^, while on the east it is 15^ or 2(P. In the latter place it
forms a small, almost triangular area, of which the base is toward the
\vest. The fracture determining this canon was probably the result of
a told, which may have been caused by igneous action, contemporane-
ous with the elevation of the tnichytic hill opposite the moiUh of the
132 OEOIiOGICAL SURVET OF THE TERRITOKIE8.
creek. Between the canon and station No: 38 there are two areas of
trachy tic rock^which may also have bad something to do with it. On the
sonth side of the Grand Canon the Dakota group does not appear at
the npper end, shales of higher positions abatting against the schists,
as shown in Fig. 2, Plate VII.
In the angle included in the great bend of the Gnnnison, opposite the
month of Smith's Fork, the sandstones of No. 1 form the surface. Sec-
tions across this area are shown on Plate Yllly the letters giving tbe
lines on which they are made, as represented on map B. On the west
side of this area the beds dip steeply, and in the valley of the Uncom-
pahgre the Dakota group is covered with the overlying beds of later
origin.
A short distance above the mouth of Koubidean's Creek it appears
again, forming bluffs that gradually rise as we go down until the river
is again in canon (Unaweep Canon.)
The following is a section of the bluff on the Gunnison opposite the
mouth of Roubideau's Creek :
No. 12. — Section of Vretaceaus No, 1. — Bluff on Gunnison River.
TbiclnMM
Top. Ft In.
1. Space reaching from the top of the blaff, which is covered with bowlders
of sandstone and volcanic rock, underlaid, in all probability, with sand-
stones and shales 50to60 0
2. Massive yellow sandstones 10 0
3. Space in which the upper part is occupied with gray and rust-colored
sandstone shales, with carbonaceous material. The lower portion of the
sp^Loe is probably filled with layers similar to those above. The slope is
covered with the debris of sandstones in which there arefragmental im-
pressions of stems, bat no leaves, although careful search was made.. 31 0
4. Oray laminated sandstones 33 0
5. Black carbonaceous or lignitic shales with etiOioresence of alkali 1 6
6. Yellow and gray shaly sandstones 4 0
7. Fine black carbonaceous shales 6 0
8. Massive gray sandstone 10 0
9. Shaly sandstones alternating with shales like those of No. 5 22 0
10. Coarse, white, granular siliceous sandstone 2to 4 0
It. Sandstone shales reaching to the base of the bluif 16 to 18 0
Base I
Total, alx)ut 199 6
This represents only a portion of the No. 1. The river, however, soon
cuts through to its base. The area occupied along the eastern side of
the Gunnison by tbe Dakota group is limited to a narrow belt, the
higher beds outcropping in low blutfs from three to Ave miles from the
river.
A section at station 60 is given below :
No. 13. — Section of No. 1 Cretaceous. — Bluff on east side of Ounnisan
Biverj Station 60.
ThieknMB.
Top. Ft. In.
1. Kassive yellow siliceous sandstones, with indistinct impressions of leaves
and stems. The sandstones are so coarse that nothing recognisable
could be seen 54 0
2. Bine argillaceous shales, gypsiferous 6
3. Fine black lignitic shales with interlaminated sandstones and clays 16 6
4. Blackish-gray laminated sandstones and shales 31 B
5. Soft gray sandstones with greenish shales in the upper part S5 4
6. Soft argillaceous sandstone shales in bands of red and green colors alter-
nating 25 4
7. Yellow siliceons sandstones in rather massive layers, very much like those
in No. 1, given above 63 0
8. Blue and yellow mottled argillaceous sandstone shales 6 4
9. Fine red and green shales, argillaceous and probably calcareous 5 10
PIAU.]
GEOLOGY SECTIONS OF DAKOTA GROUP.
133
Thickaeas.
Ft. In.
47
6
8
19
0
0
6
4
8
24
0
0
> 68 6
43
10
1
0
0
6
30
10. Compact, fine-ii^ined, brownish-red sandstones, with interlaniinatod
shaly beds with a cross-l'ractnre
11. White, dendritic, argillaceous sandstones, indurated near the top, and
having a &harp, concboidal fracture
12. Greenish and purplish argillaceous shales
12). Yellow siliceons sandstone, rather massive in the lower part, laminated
above
14. Reddish and whitish-green mottled sandstones, grading np into soft
shales
15. Reddish, purplish, and greenish sandy shales, mottled
16. Qreenish-white, argillaceous sandstone, weathering into* rounded
masses like bowlders
17. Brick-red shales mottled with green
18. Pink sandstone, 1 foot
19. Greenish shaly sandstones, with hard bands of sandstone at intervals,
and fine red shales in laminie, 6 inches in thickness
20. Soft greenish conglomeritic sandstone. The upper bed is a green sand
stone, below which is au irregular mottled limestone, argillaceous,
brown, reddish, and greenish, with jasper in centerof nodules. In the
center there are also quartz and calcite. Some of the beds in this space
are concealed
21. Massive yellow siliceous sandstone, coarse in places, with siliceoos peb-
bles
^. Soft white sandstones, conglomeritic at the base, containing black, red,
and yellow pebbles; very fine
23. Soft shaly beds, pattially concealed by argillaoeoas debris. These beds
are composed of greenish-jp>ay, argillaceous sandstones, brownish nod-
ular limestone, and greenish clays. Nearly all the beds are f|;ypsifer-
oos. The sandstones break into rounded pieces. The ddbru is coated
with a salty, alkaline efflorescence
24. Space in which the slope is partially covered with d^brig of hard red
sandstone and dark gray sandstone, and indurated argillaceous beds
of a purplish sandstone ; near the top was an outcrop of dark browu-
ish-gray sandstone. In the debris below I found a specimen SasMifraSj
like S, ndralnle^ in a rock similar, but was unable to find any fossils in
place
25. Yellowish siliceons sandstones, generally in massive beds, but toward the
base somewhat laminated
Base.
Total about
I think it likely that most of the argillaceous beds given above in
the section are calcareous. I had no means of testing them on the spot.
The nodnlar bed of limestone in No. 20 is identical with that in No. 7
of the section No. 11 at station 73. The jaspery pebbles are the same.
They are bright-red and have calcite in cavities in the center of irreg-
ular masses. The calcite is deep yellow.
There is a partial outcrop of the Dakota group in the bluff between
the Gunnison and the Grand at the mouth of the latter. The following
is the detailed section at this point :
No. 14. — Section of No, 1 Cretaceous, — Bluff on Ounnison near the mouth.
Thick neM.
Feet
1. White siliceous sandstone at base of bluff. Thickness conld not be ascer-
tained, only upper part showing
2. Fine black lignitic shales 5
3. Gray siliceous sandstone with shaly beds '
4. Beds of soft friable lignite with bands of dark greenish-gray sandstone
filled with fragments of stems and carbonaceous material. These
sandstones are in bands of one foot to two feet thickness. The lig-
nite is of poor quality, decomposing rapidly on exposure to the at-
mosphere
5. Yellow siliceons sandstones with massive structure below and becom-
ing shaly above. The lower portion is gypsiferous
> 150 tu 160
Total 155 to 106
134 GEOLOGICAL SURVEY OP THE TERRITORIES.
The lignitic beds No. 2 in this section correspond with No. 2 in the sec-
tions made near Boubidean's Creek and station No. 60 (sections Nog.
12 and 13). In the section made near station 73 (No. 11) this layer
seems to be absent, as it also is in the section made at station 14 on
Boaring Fork.
It is probably this bed that Dr. Schiel refers to in the Oeological Re-
port of Captain Gunnison's exploration when he says : '^ In the Valley
of the Blue Biver, a coal-measure, supported by sandstone, crops OQt
at several places, but the coal does not seem to be of good quality."
Professor Newberry gives the following detailed section made in
Arizona :
Feet
1. Coarse yeUowish sandstone, with concretions of oxide of iron, and obscure im-
pressions of dicotyledonous leaves 16
2. Impure coal, alternating with bauds of bitnminous shale and fire-clay, con-
taining fossil-plants — Claihrttpteri$, CyclopteriSt Sphenopteria, PSeopteris,
A;c. — ^all new species 12
3. Fire-clay and shaJe 3
4. Coarse, compact, white concretionary sandstone (i
5. Green marl 25
6. Bright red marl 22
7. White, soft, saccharoidal calcareous sandstone to base
Layers 3 to 7, inclusive, are probable Jurassic.
At another point, not far distant from where the' section above was
made, Professor Newberry made another section, of which the followiug
is a portion :
Feob
1 1. Coarse light-yellow or whitish massiye sandstone l^
Is^. Green shales, with bands of ferruginous sandy limestone and beds of lignite.
In this group at Oraylee and Camp 9G are Pinna f lingula (u. sp.) and
Gryphosa pitcheri ; and over the lignite beds are impressions of leaves of
PlotanuSf Alnus quercu», &.C., and fossil ferns of the genus Sphenopteria .... 90
13. Green, blue, and gray argillaceous shales, with bands of brown or 3-ellow sili-
ceous limestone, containing Antmonitea perlcarincUuSt Inooeramua crispii, and
Crvypihcea pitcheri, var. navia ...... 160
14. Coarse yellowish sandstone, precisely like Nos. 9 And 11 (base of Cretaceous
formation?) 25
15. Lignitic, (Jurassic T) better than that above, to base.
The bed of lignite, which he marks Jurassic? is the layer marked No. 2
in the first section given above, while No. 14 corresponds with No. 1.
Gompariug these sections with those I made on the Gunnison Eiver,
the litbological similarity is evident.
I think it probable that his beds of lignite, marked No. 12 in the sec-
tion given above, are identical with the layers included under No. 3 in
my sections on the Gunnison (Nos. 12 and 13). If so, the bed of lig-
nite which he considers as Jurassic is wanting iu my sections, while bis
layers, marked Nos. 13 and 14, correspond to those included in Nos. 23,
24, and 25 in section No. 13, made at station 60. It is a curipus coinci-
dence that the thickness given by him (185 feet) is the same as that given
by me. This, however, is no positive proof of identity, as these beds
vary iu thickness in localities* very close to each other.
If the beds do not belong to the same horizon, I have placed the line
of division between the Cretaceous and Jurassic layers lower than Pro-
fessor Newberry has done. The specimen of Sassafras that I found in
bed 24 of section No. 13, is the only evidence I have upon which to
ground such a separation.
Speaking of the specimen Pecopteris that he found in the lignite bed
(No. 2 of his first section given above), Newberry says, "Associated
with Glathropteris of Jurassic affinities, and with the first appearing
species of the dycotyledonous plants of the Cretaceous epoch, this
PKALiLj GEOLOGY CRETACEOUS NO. 2 AND NO. 3. 135
Peoopieris confirms the inference derived from other sources, that the
lignite bed containing it lies just at the poiut of junction between the
Cretaceous and older rocks, and showing a mingling of forms belonging
to the two formations, proving the impossibility of drawing sharply the
liues of division."
In the bluffs, at the month of the Gunnison, below the lignitic beds,
I found a specimen of Scaphite^ which marks the layer of Gret^iceous
age. It probably represents the equivalent of layer No. 13 in the second
section given above by Newberry. If so, the identity of the sections
with mine would seem to be pretty clearly indicated.
MIDDLE CRETACEOUS.
As I have already indicated, it is impossible in our district to give the
exactlimitsofthedifierentformationscomprehendedunderNo. 2toNo. 4,
inclusive. As the shaly character prevails throughout the series, I have
included them all uuder the same head. At the base in No. 2 they are
decidedly arenaceous, the beds just above the Dakota group beiug
lainiuated sandstones. Gradually they become more and more argilla-
ceous, and near the top thin bands of limestone appear.
Cretaceous No. 2 and No. 3.
Exposures of the Fort Benton group and the Niobrara division are
8een in the valleys of the Grand and Gunnison Rivers, and on the North
Fork of the Gunnisoii. Want of time precluded the possibility of mak-
ing a complete section from the base of the series to the top, although
1 sncceecled in getting several sections which will give the general
characters of the strata. The layers of No. 2 were not generally so well
ex|)osed as those of No 3. The higher we go in No. 2, as exposed in our
district, the moie shaly and argillaceous do the beds become, and in
No. 3 they are also calcareous.
Eagle River. — On the north side of Eagle River, opposite the second
caiion, as viewed from the semicircular ridge of stations 6 and 7, the
Fort Benton group and succeeding divisions of the Cretaceous are seen
outcropping in the most beautiful manner, as shown in Plate II (be-
tween b and c). On the south side all have been removed except a few
remnants of No. 2, and perhaps also of No. 3 in places, leaving the sand-
stones of the Dakota group as the floor of the semiquaquaversal already
described. Still farther south, in the circular area of Cretaceous near
the Eagle (see map A), remnants of No. 2 and No. 3 are seen, as shown
in the section in Fig. 1, Plate I.
Grand River. — In the range of hog-backs, extending from the Elk
Mountains along Roaring Fork and Grand River, and finally crossing the
latter, there are exposures of all the Cretaceous strata above the Da-
kota group. There was no opportunity here to make any sections.
On the south side of Grand River, in low blutfs above the mouth of
the Gunnison beds of No. 2 and No. 3, outcrop, black shales prevailing.
Ounnison River. — Under the rhyolitic and breccia-covered areas, bor-
deiing the Gunnison above the Grand Canon, there are in all proba-
bilit}' fragments of formations No. 2 and No. 3. They are exposed be-
neath the mesas that stand between Slate or East River and Ohio Creek.
The exposures of the beds immediately above No. 1, between the North
Fork of tiie Gunnison and Rock Creek, will be referred to by Mr.
Holmes, in his report on the geology of the Elk Mountains.
Between Smith's Fork and the North Fork of the Gunnison there is
/"
13G GEOLOGICAL SUBVET OF THE TERRITORIES.
wide area, in which the strata almost entirely belong to No. 2 and No. 3.
There are two parallel lines of bluffs, the first coin|>osed of black
shales, which are also shown along the coarse of the North Fork. Some
of the upper beds may belong to No. 4.
The following is a partial section on a line between station 38 aUd sta-
tion 80.
Section No. 15.
ThickiMa.
B«M. Fl In.
1. TracbytOf aboat 75 feet thick
2. Grav and black argillaceous, with JnoceramiM 58 0
3. Shales and bin ish slates 100 0
4. Slope covered with d^bria of shales above 326
5. BInish slates weatheriog rust-color, in laminae i of au inch thickness, con-
taining Inoceramua and iish-scales, too indistinct for identification 160 0
6. Gray and grayish-blue limestone with interlaminated shales, containing JmK
ceramus and fish-scales 160 0
7. Dark bluish and black shales 243 0
Total, about 753 6
At the base of the mesa, which ends east of the Gnnnison below its
month, No. 2 and No. 3 ontcrop. The following section was made north
of the Gnnnison, opposite the mouth of Roubideau's Creek. It will give
the characters of the beds. They may all belong to the Fort Bentou
group, or the upper portion of the section may possibly represent a part
of the Niobrara division.
Section JVb. 16. — Ounnison River j opposite Boubideau?8 Creek.
Thicknem.
Base. Fl In.
1. Sbaly sandstones, with interlaminated argillaceous beds extending from'
the top of the bluff on the river to the base of the first bluff north of the
river. The beds are for the most part concealed > 175 0
2. Course yellow sandstone, with calcite
3. Gray laminated sandstone
4. Thin laminsB of grayish sandstone shales, with fine black argillaceous
hhales, gypsiferous and calcareous, containing InooeramuSf Ostrea lugubria
(Conrad), and other Cretaceous fossils 125 6
5. Yellowish sandstone shales, with quantities of Jnooei'amiM and Ostrea espe-
cially abundant near the top, where there is a layer of black shales 40 0
6. Black argillaceous shales, partly concealed by debris 3d0
7. Coarse yellow, gypsiferous, and calcareous sandstones, with layer at top,
breaking into pencil-like pieces one to two inches long and an eighth of
an inch in thickness 50 3
8. Sandstone shales i 130 d
9. Fine black argillaceous shales S
10. Coarse yellow calcareoussandstone, resembling that described under No. 7. 1 0
11. Fine black argillaceous shales, with bands of sandstone ( fossil iferous), spe-
cies oi Inoceramua and Oatrea 36 0
12. Hard gray sandstone 10
13. Very fine, soft, black argillaceous shales, with a few laminro of gray sand-
stone. In the lower part of the group the shales arc coal-black, but as
we ascend they become gray-black. Nearly all the layers are fossilifer-
ous. Among the forms are Prioncifclua toyomingenaia^ Scaphitea warren-
ana, and Inoceramua problematicua. Tboy are especially abundant near
the top 66 6
14. Fine gray and yellowish shales 34 0
15. About 17 feet of gravel, composed largely of basaltic bowlders, forming the
top of the bluff
Total, about 667 8
Near station 73, on the Gunnison, shales belonging to formation Na
2, ontcrop l)eneath the breccia that underlies the rhyolitic covered
inesa. (c, Fig. 1, Plate XIV.)
nxuL] GEOLOGY CRETACEOUS NO. 4 — ^UPPEE CRETACEOUS. 137
They are 25 to 30 feet in thickDess, and represent bat a portion of the
gronp.
Under station 79, on the south branch of Smith's Fork df the Guuni-
80D, there is a greater thickness exposed, some of No. 3 probably show-
iDg, although I cannot be certain, as I had no opportunity of making a
section. These strata are the direct prolongation of those exposed in
the open country between the North Fork and the north branch of
Smith's Fork of the Gunnison.
CRETACEOUS NO. 4.
Unfortunately opportunity did not offer to study in detail the strata
referred to the Fort Pierre group and the Fox Hills beds. I was unable
to tell where No. 3 ended or No. 4 began ; the thickness, therefore,
could not be given. I estimated the thickness of the series from No. 2
to No. 4, inclusive, at from 1,500 to 2,000 feet. The only fossils obtained
were specimens of Avicula linguaformis and InoceramuB bardbina, from
an outcrop of bluish indurated clay in the valley of the Gunnison, ueHr
Kahnah Creek, beneath station 58. This layer, I think, belongs to forma-
tion No. 4. No. 4 and No. 5 outcrop in all the localities where Nos. 2
and 3 are seen, with the exception of station 73, where No. 2 alone is seen
beneath the breccia, the other beds having been eroded previous to tLe
deposition of the breccia. The best exposures are seen in the valley of
the Gunnison, but even here the softness of the beds renders them re^idily
eroded, so that they are concealed by the debris of the strata, and it is
difScult to make a connected detail- section. The strata of No. 4 are
largely light gray and bluish argillaceous beds, with sandstones near
the top that give a yellowish dSbris. They pass gradually into the sand-
stones and shales of No. 5. In No. 5 the arenaceous character prevail a.
The group next to be described may belong in part to No. 5, or may,
perhaps, be an extension of it. Until fossils are found in it, its position
is somewhat indefinite, and I have therefore considered it separately.
UPPEE CRETACEOUS.
I bad no opportunity of estimating the entire thickness of the beds
included under this group. In the Elk Mountains, where they are seen
post extensively, there has been so much disturbance of the strata that
it is difficult to obtain connected sections.
On Goal Creek there is a bluff in the face of which are exposed 1,500
feet of light-gray and yellowish sandstones and shales. On the North
Fork of the Gunnison, the exposures must be of greater thickness. The
ppper part of the series, however, is not shown here. The coal occurs
io the lower part of the series, as shown on Coal Creek. The sections
will best illustrate the character of the beds. In the broad valley ease
of station 48, and south of Grand Biver, are chocolate-colored shales,
and greenish and gray sandstones that should probably be referred to
the up[)er part of the series. The following is a partial section made
on a small branch of the Grand, below station 19.
No 17. — Section south of Grand River.
Base. TbiokoeM.
Feet.
!• Coarse soft whitish sandstoue 3
2. GreeniBb sandstoDe, coarse and soft 4
3. Hard brownish limestoDe i
4. Space covered with a reddish-brown dihris, probably underlaid by al- >.. 15
terDaiiag sandstooes and limestones )
138 GEOLOGICAL SURVEY OP THE TERBITORIES.
Baae. Tbickinsa.
Foet
5. Light gray sandstone 1
6. 8pac« covereh with a brownish d^brU in which aro nodular maeses of brown
limestone ; near the center of the space is a band of white s&ndy debris.^ 45
7. Black argillaceons shale ( 5
8. White sandstone J
9. Space covered with debris, in which are occaeional ontcrops of black and
reddish shales 26
10. Rather massive light greenish -gray sandstone 3
11. Greenish and purplish shales 6
12. Bluff of yellowish flandstone, massive below, becoming shaly above, con-
taining fragments of stems and leaves 104
Total, about 217
In layer No. 12 I found an indistinct Aralia, which Professor Lesqnerenx considers
Cretaceous. The section on station 26, still farther south, was given in chapter III.
On the ridge dividing " Oh be Joyful ^ Creek from Anthracite Creek,
near station 32, I made the following section^ the letters correspouding
with those in the illustration in Plate X :
Section No. IS.— Head of "0 he joyful^ Creek.
TfaickneM.
Base. Feet. In.
1. Massive white sandstone, reaching from the base of the cliff for sev-^
eral hundred feet I
£. •{ 2. Gray shales, succeeded by massive sandstone ^ 500 0
3. Black shales and rusty sandstone I
4. White sandstone succeeded by hard bluish sandstone J
5. Bluish-gray laminated sandstones 7 9
6. Couglomeritic sandstone, gray below, becoming yellowish toward
the top. There are pebbles of red Jasper 15 U
7. Purplish and yellowish argillaceous shales 11 6
S. Metamorphosed conglomerate 3 0
9. Metamorphosed sandstone, white and greenish below, purplish above ;
D. \ someof the layers are couglomeritic 77 9
10. Fine-grained, very compact, purplish sandstone, breaking into small
cubical blocks 4 5
11. Greenish and purplish argillaceous shales, in thin lamine 11 10
12. Purple sandstone resembling that of No. 10, more laminated at the
top 42 0
^13. Purple and yellow argillaceous shales 10 0
C. 14. Greenish trachyte in massive layer 18 0
15. Greenish and gray shales, partly ai-gilJaceous 11 B
n i 16. Dull greenish coarse sandstones 17 0
^ 17. Greenish and purplish mottled sandstones, generally compact, break-
ing into irregular pieces ; some layers are conglomeratic 35 0*
18. Compact purple sandstones, in bauds of eight iuchcs to a foot thick-
ness, breaking at right angles to the plane of deposition. On the sur-
faces quartz crystals are numerous. This bed forms the top of the
bluff 88 0
Total, about 883 8
Most all these sandstones have a metamorphosed appearance, and
the ridge in which they are exposed is intersected with dikes, which
will be described in a subsequent portion of the report. Below the
strata of the section just given there are probably 1,000 feet of shales
nnd sandstones to a series of coal-beariug strata on ^^Oh be Joyful^
Creek. The latter, according to Mr. Holmes's estimates, is about 2,OO0
feet above the Dakota group. The upper portion of these beds may
possibly have to be referred to the Lignitic group, but for the present
1 refer them to the Upper Cretaceous.
On one of the small southern branches of Anthracite Creek, near its
Lead, is an outcrop of anthracite coal. We found the float iu the creek-
3
I
X
\
I
4 I K W _.
/ •
lihrttry
( •' . .
PKALtJ GEOLOGY — UPPER CRETACEOUS COAL. 139
beil, and followed it up antil the bed was reached, near the head of the
stream. The original discovery was made, I believe, by prospectors.
The existence of coal of a good quality in the Elk Mountains has been
known for several years. In the report for 1873 (page 259) I referred to it.
The coal was exposed on both sides of the creek, the dip being nearly
in the direction of the coarse of the stream, inclining about 25^. The
beds are tipped up against the Trachytic range that forms part of the
divide between Anthraicite Creek and Ohio Creek. The coal is in a
bed from 4 to 5 feet thick. The following is the section from the coal
down : •
1. Coal, 4 to 5 feet thick.
2. Black slates and shales, with interlaminated dark sandstones,
reaching to the creek-bed, about 150 to 200 feet thickness in all.
Above the coal is a bed of sandstone, brownish near the coal, becom-
ing lighter colored as we ascend. The sandstone is succeeded by light-
gray sandstones and interlaminated dark shales. About 100 feet above
the coal is a layer of porphyritic trachyte, which inclines with the sedi-
mentary beds. It is probably an intrusion, as it resembles closely the
trachyte from the various eruptive masses in the surrounding country.
It contains iron, which gives it a rusty appearance on weathered sur-
faces. The coal will be referred to in a subsequent part of the report,
when analyses will be given. Coal Is also found on Coal Creek, and at
the head of Slate Biver, and on Kock Creek. It is all probably of the
same age.
In sandstone shales, near Mount Marcellina, I found a specimen of
Ferrea stembergii. Although I searched carefully, this ^\as the only
fossil I could find that was distinct enough for identification. This and
the Aralia I found in layer 12 of section No. 17, on Grand River, are
the only fossils found in the series and do not warrant any definite con-
clasion'as to their age.
The beds in section No. 17 have probably their equivalents in section
No. 18, but in the latter they have been so changed tbat we cannot say
80 with any certainty.
I have already referred to the possibiliry of a portion of this group
being a part of the Fox Hills beds (No. 5). A part, also, may belong to
the Lignitic group, (so named east of the mountains.)
Since writing the above I learn from Mr. Marvine that he found a
ooalbearing series of shales above typical si>ecimens of No. 4 Oretace-
•OS, and that above the coal he obtained fossils referred to No. 5 by
Prof. F. B. Meek.
Dr. Endlich also found coal above No. 4 in the Cretaceous.
It is therefore probable that the beds I have, for convenience, de-
scribed as Upper Cretaceous belong to No. 5.
From the lowest to the highest beds exposed in my district I could
find no nucouformability.
y
CHAPTER VII.
STBATIGBAPHY — CENOZOIC FORMATIONS.
vX
Id the present chapter I shall take up the remainlDg members of the
sedimentary series as exposed in onr district. These consist mainly of
beds referable to the Green Biver and Bridger groups of the Tertiary,
and I shall consider them without entering into any extended discnssiou
as to the exact names that should be given them, whether Eocene or
Miocene. Professors Cope, Leidy, and Marsh consider them Eooeue^
basing this conclusion on the discovery of vertebrate organic remains;
while Lesqaerenx refers there to the Miocene from his investigations of
their fossil flora, calling the '^Lignitic" group Eocene. I shall simply
describe the beds, giving the local names of the groups to which they
are referred.
In regard to the ^'Lignitic" group, I am unable to present any details.
Farher discussion as to the exact age of the group will l>e found in the
other reports.
As to the Post-Tertiary formations, I am able to speak only in the
most general way, and am unable to separate them into groups.
«
TEBTIABY.
Above the beds characterized as Cretaceous by their lithological pe-
culiarities and the occurrence of typical fossils, is a series of b^s from
7,000 to 8,000 feet in thickness, covering a large area extending from
the Grand Biver to the Gunnison beneath the basaltic plateaus west of
Bearing Fork. This area is marked on map E.
The best exposures are seen on Plateau Creek. I had time only to
make a partial detailed section. The strata are conformable to the un-
derlying Cretaceous, and it is difficult to determine where one forma-
tion endsand the next begins. I have arbitrarily chosen as the base of the
Bridger series a bed of red sandstone that is tolerably persistent beneath
the variegated beds above which the fossils were found. Another year
I hope to define the limits of the formation. The lower portion of the
series is referred to the Tertiary with some hesitation, as the fossils,
which were few in number, were found too far above to predicate any-
thing very definitely. Before entering into any description of the groups
as they occur in our district, I will give in tabular form the various
views held by different authorities in regard to the beds that have beeu
referred to the Tertiary formations with the exception of those I'eferred
to the Pliocene.
140
PIALE.J GEOLOGY — FORT UNION OB GREAT LIGNITIC GROUP. 141
Fart Union or Great Lignite group.
Local ty.
At Fort UnioQ, Fort
Clark, and under
tiie White Biver
beds, on the North
Fork of the Platte
Biver. above Fort
Laramie, and west
of Wind River
Mountains.
Upper Miaaoari re-
gion.
Eit^naion into Brit-
ibb America.
Porcnpine Creek,
Mianonri Cnteaii,
West Sonria Biver,
•ad other parte of
Britiah America.
Vilk Hirer
Tbnipie Hirer
Bastern baae of Black
Hflla.
Grand River, Ne-
braaka, (now Da-
koto.)
LiKoite of Long
Lake. Nebraaka,
(now Dakota.)
I*imite of Big Horn
Monntnina, and at
month of Big Horn
fiirer.
Ms beneath White
Kirer beda, aouth
of Fiort Fetterman.
Korth Platto River
and La L'r61e Creek.
Deecription of strata
Beds of clay and
sand, with round
lermginona con-
cretions and nti-
moroua beds and
seaius and local
deposits of lignite.
Age.
Eocene Tertiary . .
Tertiary
Meek and Hay-
den.
Miocene Tertiary
Lower Tertiarv . . .
...do
. ...do
Lower Tertiary...
Hayden
Leidy
Miocene
LeConte
Tertiary
Hayden
Cone
Cretaccoas ■
Miocene
v/ v^v ..........
Newberry
Hayden
Tertiary
Miocene
Newberry
Cope
Cretaoeooa No. 6 . .
Lower Eocene
Lesqnerenx...
Eocene
G. M. Dawson
Cretaceous
J.J. Stevenson
Eocene
Lower Eocene . . .
Lignitlc Tertiary
.do
do
Cretaceoaa.
do
do
Lignite (Tertiary)
Eocene.
Authority.
Hayden.
G. M. Dawson
...do...
Hayden.
.do
.do
Cope.
....do
.do
Hayden.
.do
Reference.
Exploration of Yel-
lowatooe and Mis-
soari Rivers, under
Capt W. F. Bay-
nolda, ie59-'6U:
Geol. Beport of F.
V. Hayden, p. US.
Proceedings Acad.
Nat Sci., Philadol.
phia, 1856,p.63.
Do., p. 225.
Do., p. 113.
Transactions Amer.
Philosophical Soc,
1860.
Do.
Exploration of Smoky
Hill Bailroa<l route,
1868, p. 65.
American Journal of
Sciences and Arte,
1868, p. 204.
Transactions Ameri-
can Philoaophical
Soo.. 1869.
Annals Lyceum Nat^
History of city of
New York, vol. ix,
1868.
Report n. S. Geol. Sur-
vey of Ter., 1867-
•68-'69. p. 57.
BeportU. S. GeoL Snr-
vey of Ter., Itf70,
pp. 95, 96.
Beport United States
Geol. Survey, 1873,
p. 433.
Beport TJ. 8. Geol.
Survey, 1872, pp.
410-417.
Canadian NatnraliAt,
vol. vii, April, 1874,
p. 252.
"The Geological Beln-
tlnns of the Lignit ic
Gronpa," read be-
fore the Amoiicnu
Philo9op. Soo , Jnne
If-, 1H75.
Beport of Briti^ih
American Boundary
Survey of Forty-
ninth Parallel, pp.
6, 8, 18, 19, 86, 93, 97,
103,152.
Da, p. 186.
BopurtU.S (3eol. Sur-
vey of Ter., 1867-
'68-*69, p. 72.
Do., p. 73.
Do., p. 73.
Report U. S. Geol Snr-
vey of Ter., 18TJ,
p. 446.
Do , pp. 453-'4.
Do.,pp.4S3-*4.
Rf*portU.S.Geol Snr-
vcv of Ter., ItfJO,
P.1G.
Du., p. 22.
142
GEOLOGICAL SURVEY OF THE TERRITORIES,
F(yrt Union or Oreat Lignite group — Continued.
Locality.
Coal-beds under
White River bedA,
near Fort Laramio
and east of Kook
Creek.
Laramio plains, one
hnndred miles west
of F'ort Laramie.
Coal-beds of Carbon
and Separation,
Wyoming Terri-
tory.
At Separation and
surrounding; oonn-
try. Probably same
at Carbon, Kock
Creek, Conpor
Creek, and Creston.
Carbon Station
Lifinite beds east of
Washakie Station.
West of Washakie,
and in Bridger
Pass.
Coal-beds east of Salt
Wells.
Coal-beds o f Book
SpriDfis, and east of
Rook Springs and
Salt Welle.
Henry.' 8 Fork of
Green River.
On St Vraln's Creek,
east of mountains
in ("olorado.
Marshall Mine, Colo-
rado.
Description of strata.
ToUow, msty yel-
low, msty brown,
and drab'beds.
Ralston Creek, near
Golden City, and
Golden City.
Golden City.*.
Beds under Denver,
Colorado.
At exit of Sooth
Platte River from
monntains.
Near Colorado Springs
Hardscrabble Creek,
near Cafion Ci^y
(Cafion City group).
KearCo&onCity...
An immense thickness
of sandstones and
clays, extending
from Green River
beds to Cretaceous
clays.
Coal-beds of Raton
Hills (called Raton
Hills group).
Age.
Lignite (Tertiary)
Lignite (Tirtiary)
.do
, . . . do
Lower Eocene.
Lower Miocene
Upper Eocene .
Middle Miocene.
Middle Miocene.
Lower Tertiary..
Eocene
Lignite Tertiary.
Eocene
Lignite Tertiary.
Eocene
Lignite Tertiary
Tertiary
Eocene .
Eocene .
Tertiarj-
Eocene
Lower Eocene
Tertiary
...do...
American Lower
Eocene.
Tertiary
American Lower
Eocene.
Great Lignite
group.
Anthoiity.
Hayden
.do
.do
.do
Lcsqnerenx.
...do
do
.do
Hayden
Lesquereux.
Hayden
.do
do
.do
..do
...do...
LeConte
Lesquereux
Hayden
Hayden.
...do..
Lesquereux.
Hayden
Lcsqnerenx.
Hay<1en
Refereooe.
Report U.S.Geol Snr-
vey of Ter., 1867-
'68-'d9. p. 79.
Report U.S.Geol.S^^
vey of Ter., IKO,
p. 191.
ReportU.S.Geol 8m^
vey, 1867, '68, O, ^
190.
Report U. S. Geol. Sur-
voy, 1870,p.l38.
Report IT. S. Geol. Sur-
vey, 1871, a 306
Report U-S-GedS-T-
vey, 1871, pp. 410-
417.
Report U.S.<3eolSar-
vey, 1873, Pl 366.
American Journal of
Sciences and Arts,
vol. vii. June, liHt
Report U.S. Geol. Sur-
vey, 1870.1^74.
Report U.S. GcoLSur-
vcy, 187!,p.306.
Report U. S-. GeoL Sur-
vey, 1870, p. 74.
Report U. S. Geol.
Survey, le70, p. 71.
....Do.
Lesquereux...
... do
Report U. S. GeoL
Survey, 1870, p. 5i
Report U. S. Geol-
Survey, 1867-68
-X9, p. 127.
...Do., p.l!M.
Exploration ofSmoky
Hill Railroad ronte.
1868, p. — .
Report U. S. Gwl-
Survey, 187l,p **
Report U. S. Gc*»l.
Survey, 1867-'«^
-'69, p. 134.
Report U. S. Geol.
Survey, 1871, p. *6-
Report U. S. GeoL
Survey, 187«, pp
410-417.
Report i;. S. Geol
Survey, 1867-63
-'69. p. 137.
....Do., p. 138.
Report U. S. Ge«J.
Survey. 1873, p.**-
Report U. S. Gcd.
Survey, lH67-w
-•69, pp. 149 to IM.
Report U. S. G«J-
Surrev, 1878, p 385*
Report U. S. Geol
Snrvcv, 1»"-^
-'fi9, pp. 150 to ISO.
PiATJLj GEOLOGY — FORT UNION OR GREAT LIGNITIC GROUP. 143
Fort Union or Or eat Lignite group — Continued.
locaUty.
Raton beds
Apishpa Creek. Span*
iah P6aka,and Trini-
dad, Colorado.
Saton Pnas, Piirj^a-
tory CafioD.
Baton Mountains . . .
Coal-beds of east
ed(^ of moQUtaius
In Cnlomdo.
Fiflher'a Peak, Raton
Monntains.
Baton Mountains
Central and !Korth
Colorado,
liiznltes of Colorado
Basin.
Description of strata.
Sonth Park,northeast
of Pair Play.
Grand Elver, in Mid-
dle Park.
MoantBross, in Mid-
dle Park.
Tronblfsome Creek
and Willow Creek,
in Middle Park.
TroDblesome Creek
and Mount Bross
(Middle Park).
Middle Park, Mount
Broas.
Piaeer Monntains,
Routh of Santa F6,
K<«w Mexico( Placer
Mountain Grnnp).
Liffnitio beds of New
Mexico (at leant as
far Routh as Placer
Mountain). A n •
thracite coal.
LiKnitH beds of Xew
Mexico and San
Jnan.
Sandatones and clays
ovcrl yi n g Crata-
ceons' layers.
Yellow and gray
sandstones and
laminated arena-
ceons clays.
Age.
Cretaceons.
Tertiary,
Eocene
Lower Eocene . .
Lower Tertiary.
Eocene
American Lower
Eocene.
American Lower
Eocene.
...do
Cretaceous.
Upper Cretaceons
Lignitic Toitiary
Authority.
Lignitic Tertiary
Older Tertiai7
Lower Tertiary
American Upper
Eocene or Lower
Miocene.
Upper Miocene...
Lower Tertiary
American Lower
Eocene.
Cretaceons.
LeConto
Hayden..«..
Lesqnerenz.
do
Hayden
Lesquerenx...
do
do
...do
Cope
J. J. Stevenson
Havden .
...do
Reference.
do
.do
Lesqoorenx..
....do...
Hayden.
Lesquerenx .
Newberry
Report Exploration
Smoky Hill Rail-
road route, 1668, p.
66.
...Do., p. 153.
Report U. S. Geol.
Survey, 1871, p. 306.
Report U. S. Geol.
Survey, 1872, pp.
41(M17.
Report U. S. Geol.
Survey, 1867-'68
-'69, p. 189.
Supplement to Fifth
Annual Report U. S.
Geol. Survey, 1871.
Report U. ^. Gool.
survey, 1873, p. 366.
Report U. S. Geol.
Survey, 18T3, p. 366.
American Journal of
Sciences and Arts,
vol. rii, June, 1874.
Report U. S. GeoL
Survey, 1873, pp.
453, 454.
Proceedings of So-
ciety of Nat. Hint.,
city of New York,
2d series. No. 4,
1p74, pp. 93, 94.
Also ''Geological Re-
lations of the Lig-
nitic Groups,*' read
before Amer. Phil.
Soc., June 18, 1875.
U. S. Creot. Survey
Report of 1867-68
-69, p. 179.
Also Report U. S.
Geol. Survey, 1873,
p. 3d.
R<»port of U. S, Geol.
Survey of lH67-'68
-'69, p. 183.
Also Report U. &
Geol. Survev, 1873,
p. 81.
Report U. S. Geol.
Survey, 1867-118
-'69, pp. im, 184.
Report for 1873, p. 81.
Rejwrt U. S.. Geol.
Survey, 1873, p. i?2.
Report U. S. Geol.
Survey, 1673, p. 366.
Do., p. 366.
Report U. S. Geol.
Survey, ltf67-'68
-'69, p. 190.
Report U. S. Geol.
Survey 1873, p. 3C6.
Also Anier. Jour, of
Scicuct s and Arts,
vol. vii, June, 1^74.
American Journal of
Science.*) and ATts,
vol. vii, April, 1674,
p. 90.
Some of the localities iDcluded iu the table just given will be given
in some of the tables to follow. I will not attempt to account for the
discrepancies. I have quoted the opinions relative to the age of the
144
GEOLOGICAL SURVET OF THE TERRITORIES.
varioos beds, as they are given in the reports from which I have taken
them.
The next table will include the coal strata of Bear Biver, Coalville,
and Evanston, to which Dr. Hajden (Beport (J. S. GeoL Sarvey,
ISer-'eS-'GO, p. 192) gave the name of Bear Biver group.
Bear River group.
Locality.
Coalville, Utah Ter-
ritory, and Snlphor
Creek.
Jtmr Hirer City.
EraDatoo, and
Coalville.
Bear River.
Coalville and Weber
Valley.
Coalville, Bear Iliver.
and Solphnr Creek.
DeecriptioD of strata.
SandBtones and clays
Coalville aod Bear
River.
CoalviUe
Evanston coal
CoalviUe uid
River.
Bear
Snlphor Creek, near
£ear Kiver and
Coalville.
Upper beds on
pnar Creek.
Sni-
Coalville and Bear
Rivor.
CoaM>e<lfl of C o a 1 -
villo, Utah Terri-
tory.
Evanston
CoalviUe and Bear
River.
Evanaton
Alternations of gray
ami yellowish sand-
stones and sandy
shales, with black,
bluish, and reddish
clays and beds of
coal.
Thin seams and lay-
ers of dark carbon-
accoas s h a 1 o s ,
with harder thin
bands of various
colored, argillace-
o n s , arenaceous,
and calc a r e o n s
matter, inclodin^
a very few thin
streaks of coal.
Age.
Cretaceous.
Lower Tertiary,
possibly parallel
with the older
beds of the Great
Lignitic Gronp.
Tertiary? or Cre-
taceonst
Upper Cretaoeons
(So. 5), or Tran-
sitional from Cre-
taceous to Terti-
ary.
Above Cretaoeons,
No. 5, Upper Cre-
taceous.
Some foesils Creta-
ceous and some
Eoc ne Tertiary.
Cretaneons
Authority.
Eneelmann and
Meek.
Hayden
Cretaceous
Fossils Cretaceous
Eocene
do .
...do
Meek
. . . .do
...do
Clarence King
Meek
Lesqaerenx
Cretaoeons.
Cretaceous
Lower beds Creta-
ceous, upper beds
Lower Loceue f
Lower Eocene or
Upper Creta-
ceonsf
Cretaceous.
Probably equiva-
lent to Evanston
coal.
Upper Eocene
Cretaceous
American Lower
Eocene.
American Upper
Eocene or Lower
Miocene.
Cretaceous
Hayden.
Meek .
do
...do
Bannister. . .
Lesquereux
...do
Hayden
Lesquereux
....do
Reference.
Prooeedinfff Acad-
emv Nat. ScieDce^
PhtladA, April,
1860, p. 130.
Roport of U. S.
Geol. Survey for
18n7-'0»-'O, pp.
191, 19S.
Report U. S GeoL
Survey, 1870, p
167.
Report U. S. G««l.
Survey, 1870, pp.
1^, I6d.
Report U. 8. GeoL
Survey, 1870, p.
291.
Do., S96-4»9.
U. S. GeoL Exptora-
tion of Fortieth
ParaUel, voL iii,
1870, pp. 464,465.
Do., p. 458.
Report U. S. GeoL
Survey, 1871, p
376.
Report U. S. GtoL
Survey, 1871,p.
306.
Also, Snpplemeat
to Fifth Annual
Report U. 8. GeoL
Survey, 1871.
Report U. & GeoL
Sur\*ey, 18T8, p. 14-
Do., p. 437.
Do., p. 450.
Do., p. 454.
Do., p. 534.
Do., p. 339.
Cope.
Do., pp. 410-417.
Raport U. & GeoL
Survev, 1873, p. 87.
Do., p. 366.
Do.
Do., pp. 439-44S.
n^^] GEOLOGY — BEAR RIVER GROUP — BITTER CREEK SERIES. 145
Bear River group-^Gontinued.
Loeality.
Descriptioaof stratik
Age.
Authority.
Reference.
Sranston cool
Referred provis*
ioDnlly to Fort;
Union (Creta-
ceous No. 6).
Ilalf Eocene and
half Miocene.
CoDe
Do., p. 441.
American Jonmol
Evanstoa
Leaquerenx . .
•
of Scionoes and
Arte, vol. vii,
Jane, 1874.
It seems to be pretty well established that the lower portion of the
coal-beds at Coalville and Bear Biver belong to the upper part of the
Cretaceoas formation. In this place it is proper to reter to the Judith
River beds which Dr. Hayden (Report for 1867-'68-'69, p. 50) placed
below the Fort Union group. Professor Meek (Report U. S. Geol. Sur-
vey for 1862, p. 460) says, "That the Judith River beds may be Creta-
ceous, I am, in the light of all now known of the geology of this great
internal region of the continent, rather inclined to believe." In an
article on some fossils from near the eastern base of the Rocky Mount-
ains, Colorado (Bulletin U. S. Geol. and Geograph. Survey, second
series. No. 1, pp. 40, 41 ), he refers the Judith Biver beds to the upper part
of the Cretaceous. He says, " Whether they may,'' '* in the Upi)er Missouri
country, be distinct enough from the Fox Hills group to form a sixth
8ab<livisiou of the Cretaceous series, holding a position just above the
latter, or whether they ought rather to be regarded as merely an upper
member of the Fox Hills group, may admit of some doubt in the present
state of our knowledge; though I strongly incline to the latter opin-
ion. It is true, however, that they might really be properly distinct, as
a subdivision of the Cretaceous, from the Fox Hills group, and still be
so intimately related to the latter that some of their characteristic
species of fossils might range down into the same at the Colorado locali-
ties (just as some of the Fox Hills types also occur in the Fort Pierre
group below, at many localities), without necessarily proving that these
two subdivisions should not be treated as distinct rocks."
Whether or not the coal strata at Evanston are equivalent to the
coal strata of Coalville cannot yet be positively stated. The considera-
tion of these beds belongs pro|>erly to the latter part of the preceding
chapter, but as their age was for some time a matter of doubt, I have
tbonght it best to take them up here.
In the next table I present the beds of the Bitter Creek series. Dr.
Hayden has considered them Eocene or Transitional. Prof. E. D. Cope
called them Bitter Creek (Cretaceous), (Report U. S. Geol. Survey, 1873,
p. 435).
Bitter Creek series.
Locality.
Bitter Creek VaUey
HaUviUe.
Hallville. Black
Bitttes Station, and
Point of Rocka.
HallTille coal mioea. ,
Medidne Bow
Deacription of strata.
10 H
Dark clays, sand-
stones, slates, and
coal-beds.
Ago.
Lower Eocene or
Transitional,
from Cretaceoas
tu Tertiary, in
part, at le:iat.
Eoconu or Tran-
sitional.
Fossils Eocene ...
Lower Miocene . . .
Antbority.
Hayden —
do
Meek
Lesquerenx
Reference.
Report U. S. Geol.
Sarvey, 1870, pp.
75, 76.
Do., pp. IH 165.
Do., p. 89&
Report U. 8. Geol.
SarveyJ871,pL304
146
GEOLOGICAL SURVEY OP THE TERRITORIES.
Bitter Creek series — GootiDned.
Locality.
DoHcription of strata.
Ago.
Authority.
Keforcnca.
PoiDtof Rocks
Fossils above a
Meek
Do., p. 335.
Supplement to Fifth
Annual Report
1871, V. & GeoL
Survey.
Report U. S. Gcol.
Surrey, lo72, pp.
455-459.
Do., p. 4GI.
Do., p. 532.
Do., pp. 410-417.
Report r. S. Oeol.
Survey, ISTJ, p. 306^
Do.
Point of Rocks, Black
•
Soft, light -yellow-
ish, lead-gray, and
whitiah sand-
stones, with McamR
and beds of vari-
ous-colored clays,
shale, and coaL
co<il-bed, Creta-
ceous.
Lower Miocene . . .
Tertiary....
Lraquereux . . .
Meek
Bnttos, Rock
BpiingR, and Hall-
Aside from the
Dino»aurian
the organic re-
nin inn favor the
couclnsion that
it (Bitter Creek
series) is Ter-
tiary.
Same see as at
...do
Point of Rocks coal-
'RA.nnlaiflrr
beds.
Black Battes
Hallvillot 1
Lower Rocene ' T.Ai«nni>rftM _
Black 1 nttes, Hall-
American Lower
. ...do
ville, and Rock
Spring.
Point of Rocks, Rock
Eocene.
Middle Mioeene. ,
....do
Creek, and Medi-
cine Bow.
Black Bnttes. and,
Alternating beda of
hard and soft siind-
stonoA, with argil-
laceous and car-
bonaceoos strata.
Cretaceous %..
American Lower
Eocene.
•
Cope
Do., pp. 434. 435-439.
American Jonma] of
urcstward. Rook
Spring, Point of
Bocks.
Lo'^v'er Lignite of
Black BdIU«.
Lesqnereux...
,
ScienccH and Arts,
vol. vii, Juno. Itfll.
WaskaMe group.
Locality.
Between Creston and
Bitter Creek.
Between La Clede,
Bari-clSDriiigs. and
at Barrel Springs.
Above coal-beds near
Black Bnttes.
Beds above coal-beds,
west of Separation
and extending to
the high hills of
Bridger Pass, from
the Seminole and
Sweetwater ranges.
At Separation, and
westward from
Separation above
coal-beds.
Barrel Springs
Description of strata.
Fresh-water beds
with some seams of
impure lignite.
Laminated chalky
clays ; somber, hanl,
1 ndnrated, rusty,
arenaceous clays.
Indurated arenace-
ous clays.
Age.
Authority.
Middle Tertiary.
Upper part may be
an extension of
the Bridger
group or synchi-o-
nous with it.
Middle Tertiary ..
Washakie group..
Separation to Bitter
Creek.
Miocene
Fossils Miocene.
Fossil plants,
Upper Miocene.
Fossil plants,
(Washakie group,)
Lower Miocene.
Upper Eocene
Hay den.
.do
.do
.do
Tertiary
Upper Tertiary . . .
Middle Miocene . .
...do
Meek
Lc»qucrenx
do
....do
Meek
Bannister..
Lesquereux
Reference.
Report U. S. Gwl.
Survey, lJiC7-'t»-
'l.'J, p. *1V0.
Report U. S. Geol.
Survey, IdTO, p. 73.
Do., p. 71.
Do., p. 138.
Do , p.l64.
Do., pp. S96, 909.
Report U. S. Geoi.
Survey, 1871, p. 306.
Do.
Report 0. S. Ged.
Survey, 1872, pp.
410-417.
Do., p. 457.
Do., p. 5S5.
U. S. Geol. SorrtJ
Reports, 1673, PL 306-
muLl GEOLOGY ^WASHAKIE AND GREEN RIVER GROUPS.
147
As we have already seen, Cope conaidera the Bitter Creek sericH Cre-
taceoas. In a letter to me be says, " 1. have never seen any certain
correlation of the Bitter Creek with the other lignite beds, so I call it
No. 6, with a question, although it may be a No. 7." Of the Washaide
group he says, *' 1 have never studied the Washakie group, and do not
know where it comes in.'' Prof.F. B. Meek (Report U. S. Geol. Survey,
1872, p. 457) says, *' In the latter (Washakie group), so far as our pres-
ent knowledge extends, only fresh- water and land types of fossils have
yet been found, and we have always regarded it as being of Tertiary
a^e. Exactly where the one ends and the other begins we did not see."
*' Between Black Butte and Bitter Creek stations (separated by a distance
of only six miles by a right line east and west) we observed no marked
change of lithological characters, from the Bitter Creek series to the
Washakie group, while the two series seemed to be conformable in dip."
Dr. Hayden (Report U. S. Geological Survey, 1867-'68-'69, p. 190)
says, " From Creston to Bitter Creek there is a series of purely fresh-
water beds, with some beds of impure lignite, with vast quantities
of fossils belonging to the genera Unto, Melania, Vivipruj Helix, &c.
This group I regard as Middle Tertiary, and the strata are very nearly
horizontal. I have regarded these beds as separated from the Lower
Tertifir^^ or true Lignite group, and have designated them by the name
of the "Washakie group." The Washakie group, therefore, lies above
the Bitter Creek series.
Wahsatch group.
Locality.
Description of stratA.
Age.
Authority.
Reference.
1
Wevtof Fort Bridger . . Vflripcrated s a n d a
Tertiary
Hayden
Report U. 8. Geol.
Survey, 1867-'6d-C9,
and clays, some
shade of red pre-
p. 19L.
dominating ; very
little calcareous
matter.
Went of Carter Sta-
Rod, indurated. are-
Beneath the Bridg-
....do
Report U. S. Geol.
Sorvov, 1870, pp.
tion, and from niiceoiis clays, with
er gronp, and
Bridj^er Station to ' beds of graviab aod
probably s y n ■
147, 148.
Atpen. 1 rrddish-frniy sand-
chronous with
' atone altomatine.
the Green River
Pinkish and parp-
group.
linh clays aro the
dominant features.
Head of Echo Canon . Reddinh and purplisli
Miocene
. . ..do .........
Do., p. 155.
indurated sands
and clava
"om Carter Station , Variegate<l clays.
Below Bridger
-••dp ^
Do., p. 168.
to the middle of, sands, and aand-
group.
Echo Ca&on. 1 atones.
On paleontological
gronnds. synchro-
CODB ..••.••...
Report TT. 8. Geol.
Survey, 1873, p. 441.
Also, Proceediuga
nous with Green
River epoch (Eo-
Acad. Nat. Sci.,
cene).
Phil., 1878, p. 279.
Oreen River gr(yi(p.
Locality.
Boat of Rock spring,
and in Green River
Valley (Green Riv-
er shales).
«e»r Fort Stam-
haogh, Sweetwater
Vtlley,Black'sFork
ofGroen River, Big
Budy, and near
Otanger Station.
Description of strata.
Thinly laminated
chalky* slates.
Reddish or India-
ocber days, with
leaden bands, yel-
low marls, and
rusty drab lime-
stones.
Age.
Middle
above
group.
Tertiary,
Washakie
Lower Miocene.
Authority.
Hayden
.do
Reference.
Report U. S G'ol.
Survey, 1867-'lte-'t9,
pp. 190. 101.
Report U. S. GeoU
Survey, 18*0, pp.
30,40.
148
GEOLOGICAL SURVEY OF THE TEREITOBIES.
Oreen River group — Continued.
Locality.
Lower part of Bridff-
er*s Butte, and oth*
er localities near
Fort Bridger.
Ho Dry* 8 Fork of
Green River.
Green Ki ver. between
Bonry'H Fork and
Black's Fork.
Green Biver beds
Gi%en Biver
East of Book Spring. .
Gi^^zzly BntteSt Hen-
ry's Fork.
Green Biver Basin.
Green Biver
Description of strata.
Limestones and
marls.
Light, ash-Golored
Mds, succeeded by
brilliant colored
strata.
Shales, marls, and
harder calcareous
strata.
Age.*
(Green Biver beds)
Lower Miocene..
Middle Tertiary.
(Older than Hsy-
don made them).
Eocene.
Upper Miocene
Probably eqaiva-
lent of the £ooeue
Tertiary.
Miocene
Eocene.
Lower Miocene or
Eocene.
Eocene
Upper Miocene.
Upper Miocene.
Lower Eocene.
Authority.
Hay den.
.do
.do
Newberry. .
Lesqaerenx
Lcidy
Lesqaerenx
Cope
Marsh
....do
Lesqaerenx
. ...do ......
Comstock
Beferenee.
Do., pp. 55, 56.
Do., pp. 58, 59.
Do., pp. 69, 70.
Do., p. 143.
Supplement to Sth
Annual Report
([871).
Beport U. S. Oeol
Survey, 1871, p 353.
Beport U. S. Geol.
Survey, 187-2, pp
410-417.
Beport U. S. GeoL
Survey, 1873, p 436.
American Jonrnal
Science and Arts,
vol. iv, 1872,p.S56.
Do., p. it99.
Beport U. 3. (5eoL
Survey, 1873, p. 366.
Amer. Jour. Science
and Arts, voL iii,
June, 1874.
Bept. of Beconnais-
sanoe of Yellow-
stone Biver sod
N. W. Wyoming,
under CapL Jones,
1675, p. 1)23.
The Wahsatch group and the Green River group occupy two distinct
basins, but are considered synchronous by Dr. Hayden aud Prof. E. D.
Cope. (See tables of Green Kiver and Wahsatch groups). I shall refer
to these groups in another portion of this chapter.
The position of the Wind River group, given in the next table, is by
no means certain. It may be equivalent to the Green River formation,
as it seems to be above the Lignitic group, or it may represent the
Bridger group. *
Wind Biver group.
LooaUty.
Description of strata.
Age.
Authority.
Beferenee.
Wind Biver Valley
and west of Wind
Biver Mountains.
Between Wind Biver
Light fsnky and ash-
colored sandstones,
with more or less
argillaceous layers.
Yellowish and lij^ht.
more or less sandv
marls, with pinlc
bands, alternations
of sandstones and
olays.
(Beneath White
Biver group).
0)
(t)
Above Lignitic
group and under
White Biver
group.
Hayden
....do
....do
Exploration of Yel-
lowstone and Mis-
souri Bivers, onder
Capt W. F. Ray-
nolds. 1859--60.
Geol. Beport F. V.
Hayden, p. 89.
Do., p. 79.
Beport U. S. GeoL
Sarvey,l867-'68-*e»,
p. 57.
and DiK Horn
Mountains.
t
mutl GEOLOGY — ^WIND BIVEB AND BfilDGEB GROUPS.
149
Wind River group — Continaed.
Loedity.
DescriptioD ot strata.
Age.
Authority.
Reference.
Sweet Water Valley
aod Wind Kiver
Brown indorated
(?)
Hayden
Report U. S. GeoL
Survey, 1870, p. 'Si.
sands, with seams
(Wind River
Moontains.
of imparo lignite or
curbonaceons clay,
with layers ol
cosrse sandstones.
group).
Between Wind River
Marls are frequently
Resembles the
Comstook
Report of Geological
and Owl Creek.
variegated, i. e..
Bridger rather
ReconnaissaDCe o f
bands of a bright
red or pinkish color
than the Green
Yellowstone River
River beds.
and l^orth western
are associated with
Wyoming, under
Captain Jones, 1875,
the blue-greenish
and ]ightKX>lored
pp. 1)28, 139.
beds.
Bridger group.
Locality.
West of Bryan and
at Church Buttes.
Capping the Green
Kirer beds in places
between Big Bandy
and Black's Fork of
Green River.
Between Fort Bridg-
er and tbe Uintah
Mountains.
Bridger's Butte, near
Fort Bridger. and
divide between
Huiith's Fork and
Henry's Fork ol
Green River.
Between Smith's and
Henry's Forks of
Green River and in
Green River Valley.
Cborcb Buttea
Echo and
Vall^a.
Weber
Near South Bitter
Creek at La C16(le.
Henij's Fork and
Mnddy Creek.
Description of strata.
Fine sands md sand-
stones, mostly in-
durated, sometimes
forming compact
beds, but usually
weathering into
castellated and
ddlnc-like forms,
like the Bad Lands
of White River.
Leaden-gray indu-
rated arenaceous
clays.
Somber-brown indu-
rated arenaceous
days, gray and
rusty-brown sund-
atones ; leaden-
brown clays.
Indorated clays ; in-
tercalated with
the clays afe beds
of rusty -brown and
gra> sandstoneA,all
tending to a con-
cretionary struo-
tnro.
Brown indurated
sands and daya.
Conglomerates .
Dull*colore<l indu-
rated clays and
brownish, dull-yel-
low, ur gray arena-
ceous layers, with
moro or less ccmcre-
tionarv structure.
Age.
Upper Tertiary . . .
Above Green River
group.
Miocene.
Bridger group
Above Lower Mio-
cene beds.
Middle Tertiary,
probably synchro-
nous with White
River bods.
Fossils, Miocene . .
Probably parallel
with Bridger
Soup (Upper
iocene).
Upper Miocene . . .
Authority.
Hayden
I bUO ••«•«<
.do
.do ..
.do
Eocene.
Upper Miocene .
Upper Eocene .
Reference.
Report of n. S. Geol.
Survey, 1867-'6ti'-^,
p. 191.
Report XJ. S. GeoL
Survey, 1870, p. 40.
Do., p. 4S.
Do., pp. 55, 56.
Do., pp. 58, 50.
. ...do ......
Meek
Hayden
....do
Cope
Lesquereux
Comstook . .
Do., pp. 144, 145b
Do., pp. 908, f299.
Do., p. ICri.
Do., p. 75.
Report U. S. Geol.
Survey, 1873, p. 437.
Report U. S. Geol.
Survey, 1871, p. 300.
Report of Reconnais-
sance of Yellow-
stone River and
Northwesti<rn
Wyoming, under
Captain Jones, 1875,
p. 127.
150
GEOLOGICAL SURVEY OF THE TERRITORIES.
White River group.
Locality.
On White River, an-
(lor Loupe River
beds, and on tbe
Niobrara River,
and acrons to the
Platte River.
On White Earth
Oeek and White
River.
In the valley of the
Chug- Water, on
Horse Cnek, and
on tho North Platto.
Beds beneath Chej'-
eiine.
On the Chnff- Water
and Crow Creek.
Along the North, and
on La Bont« and
^^orseshue Creeks.
Fort Fetterman
100 miles northwest
of Fort Laramie.
Plains woBt of Chey-
enne.
Description of strata..
White and light-drab
clays with some
beds of sandstone,
and local layers of
limestone, and
whitish indurated
clays.
Variegated beds,
cream -colored, red-
dish-brown, and
light-gray sands
and marls.
Light<colored marls
and sands.
Drab, yellow, and
light-gray sand-
stones, marls, and
days.
Age.
Miocene.
Authority.
Hayden
.do
White River Ter-
tiary.
.do
.do
.do
do
.do
Miocene.
Miocene (f)
Miocene.
.do
..do
.do
.do
.do
.do
.do
Leidy..
Hayden
Reference.
Cope Do.,p.461
GeoL Report of Ex-
ploration of Yellow-
stone and MissoDri
"Rivers, by Dr. F. V.
Hayden. nnder
Capt W. F. Rav-
nolds,1859-'60j».29:
a' so Report U. S.
Gool. Survey, 1j»7-
'6.<-'69, J). 57.
Exploration of Yel-
lowstone and Mis-
souri Rivera, ii. 134.
Report U. S. GeoL
Survey, i867-'6e-'69.
p. 80.
Do., p. 110.
Report of U. S. Geob
Survey, ItfiO, pj). 13,
Do., pp. 19,30,2X
Do., pp. 33, S4.
Do., p. 131.
Report U. Sl GeoL
Sarve3%1671.p.353.
Report U. S. GeoL
Survey, 1870, pt 17.
The "Monument Creek" and the "Gallisteo Sand" groups deserve
mention here. The latter has been referred to the Miocene bv Dr.
Hayden (Report U. S. Geol. Survey, 1867-'68-'69, pp. 139, 107, 190.) It
consists of " variegated sands and sandstones, and light-reddish brick-
red, purplish, yellow-white, brown, and drab, with irregular layers of
dull rusty-brown concretionary arenaceous limestones." It will be noticed
that this description resembles those already given for the Green Hiver
and Wahsatch groups. ^
In the report of U. 8. Geol. Survey, 1867-'68-'69, p. 139, 140, Dr. Hay-
den points out the resemblance ol' the Monument Creek group to the
Gallisteo Sand group, and to the beds between Fort Bridger to Weber
Canon (Wahsatch group), and refers it to Late Miocene or Pliocene.
He makes the same reference in the report for 1870, p. 161, In the
report for 1873, page 33, he refers it to Miocene. In Bulletin No. 3,
Second series, he refers it to the Lignitic group, but in Bulletin No. 4, p.
219, he corrects this statement. Prof. E. D. Cope (Report U. S. Geol.
Survey 1873, p. 430) says: ''The age of the Monument Creek formation
in relation to the other Tertiaries not having been definitely determined,
I sought for vertebrate fossils. The most characteristic one which I
procured was the hind leg and foot ol' an Artiodactyle of the Oredore
type, which indicated conclusively that the formation is newer than the
Eocene. From the same neighborhood and stratum, as I have every
reason for believing, the fragment of the Megaceratops coloradoensis was
obtained. This fossil is equally conclusive against the Pliocene age of
the formation, so that it may be referred to the Miocene, until further
discoveries enable us to be more exact."
The columns on the opposite page are summarized from the tables that
have already been given :
rSALB-J
GEOLOGY — CRETACEOUS AND TERTIARY STRATA.
151
o
oC
S
c
'J
S
o
a
a>
a
^
«
bfl
•c
ce
a
2
Pi
u
Pi
•s
a
u
>;{)
OB
idddQ
04
P
o
I
o
>
a
P.
a
o
»4
•c
§
o
«
S<s W
£p' X
•So o
P9-3 'fa
oCnP< 6
|S5 P24
l4
P
p
•J
P U
©jg
C e«
— a
"J
p tS-g
p.
p
3
u
1 3
•3
go
u
04
p-5 CO
" to* -■* ^
^eI:2Ps£|
« "^ T* ? *3
g P^
^^iS « q 5
^ w bw "^
•9at»oo5r
JOMOT iieaiiamY
I
a
u
PQ
0
'en900iN
J9ddii
p«
p
I
p
•aippiK
p
2
•
-a,
P.P
P 2
t
9
•a
'jaAKKI
53
© -
P-i
•Sis
p
P<C o
cmJ5
*duaz2f aoiaxi "^
•c
O
PQ
'ivaopfsavjx
H
O
>
a.
p
2
a
1
•fi ox
*9a900{p[
'oaooo^
jyddxi
152 GEOLOGICAL SURVEY OF TH^ TERRIT0RIE8.
It will be seen, on referring to the column beaded Lesquerenx, that
beds of the Bitter Greek series are in part under Miocene, and in part
under Eocene. The reason of this way be that the specimens are from
diHerent horizons, or, if from the same horizon, it would seem to prove
that there is a mingling of forms in the flora of Eocene and Miocene
formations. It is probable that when more complete collections are
made, this will be found to be the case. That the coal-beds of these
localities, however, belong to the same horizon is evidently the opinion
of Dr. Hayden and Prof. F. B. Meek, who have studied the localities
stratigraphically. (See references in tables).
LIGNITIC GROUP.
West of the continental divide the coal-bearing strata are not con-
fined to the Lignitic group (as named east of the mountains). As noted
in the preceding chapter, I found lignite' in the sandstones of the Dakota
group. In 1873 Mr. Marvine* found a '^thin seam of coaP^ ^^a few
hundred feet above the quartzitic sandstones of No. 1," at the '^Hot
Springs" in Middle Park. During the season of 1874 Mr. Marvine
found coal in a horizon above fossils of No. 4 and below those referable
to No. 5. Dr. Endlich, in his district, recognized three distinct lignitic
layers in different horizons of the Cretaceous formation. The coal of
the Elk Mountains is probably of the age of the Fox Hills group. I
have already referred to the possibility of the upper part of the series
there, in which the coal is found, being a part of the Lignitic group, but,
until fossils are found, I refer it to Upper Cretaceous.
Professor Newberry t found lignite in Lower Cretaceous and in Jurassic
strata in Northeastern Arizona. In Minnesota, also, coal has been found
in Lower Cretaceous rocks.
The reason of the differences of opinion as to the age of the disputed
beds called lignitic seems to be that there are two sets of lignite-bearing
beds close together, one belonging to the horizon of the Fox Hills be<ls
of the Cretaceous or possibly a little above it, and the other belonging
to the horizon of the Fort Union group (Lower Eocene). As Prof. G.
M. Dawson I says, '* An observer beginning his btudy of the beds ou
their eastern margin, and proceeding westward, as Dr. Hayden has
done, would be completely justified in placing the whole series, at least
down to the top of Cretaceous No. 5, in the Tertiary; while a geologist
familiar in the first instance with the fossils of the underlying Cretaceous
formations, and following the lignite strata eastward from their appear-
ance in the Rocky Mountains, would in all probability include the whole
series in the upward extension of the Cretaceous, though doubts might
begin to assail him before he reached the upper or most eastern beds.''
In many places the coal of the upper part of the Cretaceous appears
to be absent. When present the sandstones have a transitional char-
acter, but this is also noticed where coal is found in the lower part of
the Cretaceous formation, and in the Jurassic, just beneath. Professor
Cope refers the lignite-beds to the Cretaceous formation from the dis-
covery of the reptilian fauna in them. He has described a Dinosaurian
reptile from the Bitter Creek series,§ and also from the Fort Unioo
group in Colorado.|| Professor Meek^] says, ^^ Aside from the Dino-
* Report of U. S. Geol. Survey, 1873, page 156.
t Colorado Exploring Expedition, Geological Report, pp. 83, 85.
t Geological Report on the Region in the Vicinity of the Forty-ninth Parallel, p. 208.
i Proceedings of the American Philosophical Society, 1872, p. 482.
II Report United States Geological Survey of the Territories, 1873, p. 444.
H Report United States Geological Survey, 1872, p. 461.
WAUL] GEOLO&Y — ^LIONITIC GROUP. 153
tanrianj tbe organic remaiDS favor the conclusion that it (Bitter Creek
series) is Tertiary." Professor Lesquereux, from the study of the tiora
as we have already seen, refers tbe beds to the Eocene period. Cope,
iu his conclusion, (Report United States Geological Survey, 1873, p. 447),
says there is, then, no alternative but to accept tbe result tliat a Tertiary
flora was contemporaneous with a CretDceous fauna, establishing an
QDinterrupted succession of lite across what is generally regarded as
one of the greatest breaks of geologic time.
I insert here a letter from Prof. Theodore Gill, on the value of the
I>ino8aurian remains, as proof of the Cretaceous age of the strata in
which they are found:
Smithsonian Institution,
Washington^ January 9, 1876.
Dear Sir : Tour letter, requesting a copy of my commnnication to 'the meeting of
the National Academy of Sciences respecting the values of fossils as indices of forma-
tions, has daly come to hand.
My remarks were not published otherwise than in brief newspaper reports. They
were elicited by the controversy then prevailing respecting the age of the lignite-beds
in which the Dinosaurian remains, to which you allude, were found. The substance of
my criticisms was that we should not be too much influenced in our views as to the
age of any gronp by one or two inclnding fossils; and I brought up a number of cases
to show how mistaken we should be if we allowed ourselves to be too much influenced
by what was known of tbe paleontology of any limited country. Among other iu<
8tau<res, I especially alluded to the fact that for a Jong time the flsh, genus Ceratodus,
was regarded an indication of a not later than Triassic age of any including forma-
tion ; and showed that while such is the case for the northern hemisphere, so far as
yet has been observed, we still have living Ceratodi in the southern hemisphere, not
long ago discovered. I proceeded then to show the close relation between tbe species
of this gronp, which lived in Triassic Europe, and the species which live in modern
Australia. I further indicated that the remains of J gat haumaSj found in the lignite-
beds, were not sufficiently characteristic to enable us to determine the exact relation-
ship of the genus, and that it was apparently not, at li-ast nearly, allied to any of the
previously recognized forms of the order. The conolnsion was drawn that inasmuch
as the same typical structure could peraist and had persisted, with shifting geographi-
cal relations, through such lon^: ages as had Ceraiodus^ that in the case of the Dinwauri-
anSf where the affinities were less intimate, there could be no a priori reason why they
might not have had a similar history. It was in fact assuming the premises in dispute
to assert that because the remains of the Dinosaurian were found in a given horizon
they most necessarily indicate Mesozoio age, notwithstanding the other associated fos-
sils. I finally urged that in this case, where the evidence was conflicting, we would
have to wait for further proof froni other quarters, and especially for the tracing of
deflnite horizons toward, and co-ordination with, those above and below the beds in
dispute.
J adduced a number of other facts bearing on the subject ; but this will be sufficient
to show the drift of my argument and the evidence of the facts set forth.
Hoping that this epitome will answer your purpose, I remain, yours trnlv,
THEO. GILLm
Dr. A. C. Pbalb.
Gope also says,* ^< The appearance of mammalia and sudden disap-
pearance of the large Mesozoic types of reptiles may be regarded as
evidence ofmiffratian^ and not of creation. It is to be remembered that
tbe smaller type^ of lizards and tortoises continue, like the crocodiles,
from Mesozoic to Tertiary time without extraordinary modification of
structure. It is the Dinosauria which disappeared from the land, driven
oat and killed by the more active and intelligent mammal: herbivorous
reptiles like Agatkaumus and Cionodon would have little chance of suc-
cessful competition with beasts like the well-armed Bathmodon and
MetalophodonJ^ If the smaller types persisted, why not the larger!
The only reason he gives is that they would have little chance of suc-
cessful competition with the well-armed mammals. Why should this not
'Report United States Geological Survey, 1873, p. 442.
154 GEOLOGICAL SURVEY OF THE TEEEITORIES.
apply also tx) the smaller f He says also tbat paleontology confirms
Haydeu's conclusiou that tbere is no evidence of any catastrophe suffi-
cient to account for any sudden and complete destruction of life. The
change from marine waters to fresh water accounts for the destrnction
of the marine invertebrate life, but, as Hay den* says, " the vertebrates
of the Lignitic period having great powers of locomotion, and being able
to live on land as well as in the lakes and marshes of that time, and as we
have shown that there was at no time any important catastrophe or phys-
ical changes sufficient to aifect them, could well have prolonged theirexist-
ence far up into the Lignitic group, carrying with them as an inheritance
their Cretaceous characters." Nooneformoflifeshouldbetak^'Qasaba^is
of classification. Cope's comparative list of vertebrate species,! under
Colorado and Dakota, includes two species of Plastomenus^ a Teitiary
genus, although in a foot-note he says he so refers them provisionally.
The fauna, therefore, even according to his own list, is not exclusively
Cretaceous. Writing to Prof. G. M. Dawson on some remains found in
the lower portion of the Lignitic formation on the forty-ninth parallel,
he says : % " Tbis is a characteristic collection of the reptiles of the Fort
Union Cretaceous, but with increased admixture of Eocene forms. Plas-
tomenus is an Eocene genus, but the reference of the new species to it is
not tinal. But you send two Eocene gar scales which have every ap-
pearance of belonging to the same formation. Will you re-examine your
notes to inform me whether they really belong to the same horizon as
the others f " Dawson 8a> s :§ *' The gar scales referred by Professor Co;>e
to the genus Clastes^ were obtained at the very base of the Lignitic
formation and below the lowest lignite-bed." " Dinosaurian bones oc-
curred within a ft w feet of them."
We have already seen that thecoal-bearingstrata at Coalville and Bear
River are undoubtedly Cretaceous. The only leason to be given for in-
cluding the different groups in one formation is the fact of the presence
of coal; and we might, then, include all coal-bearing strata, whether
Carboniferous, Triassic, Jurassic, Cretaceous, or Tertiary, in the same. In
this case the lignitic strata are very close together ; and in fact one im-
mediately succeeds the other. This is also the case at the base of the
Cretaceous in some places. Professor Newberry,|| referring to a bed of
lignite of Jurassic age in Northeastern Arizona, says: ^^The sandstone,
shales, and limestone lying above, also include many beds of lignite
closely resembling this, and on lithological grounds would appropriately
be grouped with it. In fact they have been considered Jurassic, and the
only Jurassic rocks in this region, by the geologist Marcou, who claims
to have discovered the representative of this formation in New Mexico.
Unfortunately, however, for that classification, immediately over the
thin stratum of yellow sandstone which overlies the coal, are beds of clay
shale, with bands of limestone in which are unmistakable Cretaceous
fossils." Plants of the lignite above were dicotyledonous, while those
found below ^^ are closely allied to some of those most characteristic of
the Jura and Upper Trias of Europe.'* 51 The base of the Cretaceous
formation is therefore seen to resemble the base of the Tertiary. In
Eastern Colorado the upper part of the Cretaceous is destitute of coal.
In fact the Upper Fox Hills group is wanting in many localities, and
* Notes on the Liguitic groap of Eastern Colorado and portions of Wyoming, Bulle-
tin No. 5« second series. United States Geological Survey of Territories, p. 411.
t Report U. S. Geol. Survey of Terr., 1873, p. 433.
I Geol. Report Forty-ninth Parallel, p. 200.
$ Ibid.
ji Ives's Colorado Expedition, Geological Report, p. 83.
in Ives's Colorado Expedition, Geological Report, pp. 83, 85.
MAUL] GEOLdbY — LIGNITIC GROUP. 155
sometiiues the Lignitic jsrroap rests on No. 4 or No. 3 Cretaceous.* I
have already (page 145) referred to the equivaleuce of tbe Judith liiver
bed.s aud some strata at the eastern base of the Kooky Mountains, west
of Greeley and Evans, Colo. The fossils upon which Professor Meek
predicated this /equivalence "came from the very upper beds of well-
defiued marine Cretaceous, and below the horizon of all the coal-bearing
strata of the Colorado region." t
In the report of United States Geological Survey for 1872, p. 459, Pro-
fessor Meek speaksof the resemblanceof some of the fossils from the Black
Butte and Point of Bocks localities, to some species found in the brack-
ish-water beds at the mouth of the Judith Eiver. They would seem, •
therefore, to be equivalent to those seen east of the mountains west of
Greeley. He says they are distinct from any found at Coalville or Bear
Biyer. In speaking of Black Butte it must be remembered that there
18 also a Black Butte station at which the beds are probably not of the
same horizon. Point of Kocks, Hallville, and Bock Spring are not all
of the same horizon. In going from Table Bock to Salt Wells (see re-
port of U. M. Bannister, U. S. Geological Survey, 1872, p. 524), we go down
through a iresh-water series to brackish-water- beds and finally to ma-
rine Cretaceous at Salt Wells, which is in an anticlinal. Speaking of
the coal horizon of Point of Bocks, Bannister says:} ^'It seems almost
too low in geological position to be referred to the horizon of the Hall-
ville beds, although it may occupy the same." Meek, in the report
for 1872, p. 458, refers them to the same horizon, although in tbe re-
port for 1871 he refers Point of Bocks to the Cretaceous and Hallville
to the Eocene, from the affinities of the fossils.
Until the stratigraphy of the region is thoroughly inYestigate<l there
mast remain some little doubt. Professor Meek, in his table of fossils
pf-the Bitter Creek series, § evidently considers the Point of Bocks
locality at the lower part of the series. Professor Meek || has identified
some fossils from two hundred miles east of Greeley, Colo., as the same
that are found over one of the coal-beds at Hallville, Wyo., and at
Black Butte Station, Utah. He says: '^That the formation from which
these fossils came, however, is the same as the Bitter Creek series of
Wyoming, including the Black Butte beds, the Hallville coal-mines,
Point of Bocks, and Bock Spring coal-mines, &c., I have scarcely a
shadow of doubt."
It remains now to state the following conclusions:
1. The lignite-bearing beds east of the mountains in Colorado are
the equivalent of the Port Union group of the Upper Missouri, and are
Eoceue-Tertiary ; also, that the lower part of the group, at least at the
locality two hundred miles east of the mountains, is the equivalent of
a part of tbe lignitic strata of Wyoming.
2. The Judith Biver beds hav« their equivalent along the eastern
edge of the mountains below the Lignite or Fort Union group, aud
also in Wyoming, and are Cretaceous, although of a higher horizon than
the coal-bearing strata of Coalville and Bear Biver, Utah. They form
either the upper part of the Fox Hills group (No. 6) or a group to be
called No. 6.
3. That the upper part of the Fox Hills group is wanting in many
parts of Eastern Colorado, and when present seems to be thin and des-
titute of coal.
* Hayden Bulletin No. 5, 2d series, U. S. Geological Survey of the Territories, p. 404.
t Bulletin No. 1, 2d series, U. S. Oeolof^ical Survey, p. 40. \ |
t Report U. 8. Qeological Survey, p. 532.
fU. S. Geological Survey, p. 477.
IBuUetin Nu. 1, 2d series, p. 42.
15^
GEOLOGICAL SURVEY OP THE TERRITORIES.
TERTIARY BETWEEN GRAND AND GUNNISON RIVERS.
The only portion of the district in which Tertiary rocks are seen is
in the region between its two main streams, i have no absolate proof
that the Lignitic group is present. At all the localities I visited, the
intermediate beds from the upper part of the Fox Hills beds to the
red sandstone bed that I took as the base of the Green River and
Bridger series were covered. The Lignitic group may include a portion
of the beds above and a part beneath, it is impossible to define any
line of separation. Although I could see no unconformability between
the Cretaceous and overlying Tertiaries, it is probable that in other
places evidences will be found, especially on the edges of the Tertiary
basin. In a conglomeritic sandstone on Plateau Greek I found an
inner convolution of a 8caphite» It was a pebble, and proves that the
layer in which it ^¥as found, is of Post-Cretaceous age, its materials com-
ing from the disintegration of Cretaceous rock which were above water-
level when the stratum was deposited.
GREEN RIVER AND BRIDGER GROUPS.
I shall use the name Oreen Kiver group to include also the Wahsatch
group of Hayden. Cope restricts the name to the Green Eiver shales.
Whether We call them Eocene or Miocene depends upon the view we
take of the beds below. The vertebrate palentologists consider them
Eoaene, while all who hold to the Tertiary age of the Lignitic group
place them in the Miocene.
As has already been stated, the greater portion of the Tertiary beds
exposed in the district is referable to the Green Elver and Bridger
groups. These strata are seen between the Grand and Gunnison riveis,
west of Roaring Fork, and are almost horizontal, dipping slightly to the
eastward beneath the basaltic-capped plateaus, which are fully described
in other portions of the report. The area is shown on map E.
The characters of the included rocks will be given as we proceed.
The best exposures are seen on Plateau Creek, a branch of the Grand
Kiver, which joins it some distance above the mouth of the Gunnison,
after cutting deeply into the strata. The following section will give the
best idea of the succession of the strata on Plateau Creek.
No. 19. — Section of Tertiary Beds. — Plateau Creek.
TblckneM
BaM. Ft la
1. Red sandstone
2. Yellow and white sandstones
3. Red sandstone, 30 feet
4. Varief;atcd red, yellow, and bluish marlSi sandstones, and clays.
5. Bluish and black argillaceous beds «
6. Yellow sandstone
7. Black argillaceous beds
8. Brownish red sandstone ^2,000 0
9. Soft greenish argillaceous shales
10. Green sandstone shales
11. Black argillaceous shales
12. Massive sandstones in pinkish-white and yellowish-gray layers,
with ir.terlaminated greenish shales. Some of the layers are ^250
conglomeritic
13. Dark greenish sbaly sandstone
14. Series of soft variegated beds, yellow, reddish, and black, much like those
given iu lower part of this section. They are generally concealed, but
where exposed the dSbris, from the sofrness of the strata, makes it
almost impossible to get the section in detail. Thickness about 740- Q
>25(
PUUL) GEOLOGY — SECTION OP TERTIARY STRATA. 157
Thicknees.
Base. Ft. lu.
15. Space probably filled with soft yellowish sandstones and interlaminated
red and green shales and marls, a continuation upward of No. 14 170 0
16. Soft. f2;rayi8h-wbite sandstone 46 0
17. Red and greenish shales ..» 23 0
lb. Gray sandstone. 3 0
19. Greeuish-gray sandstone B 3
20. Red shales, passing up into green 3 6
21. Yellow sandstone, covered near the top, having in all probability interlami-
nated shales 75 0
22. Yellow sandstone 48 0
23. Red and greenish-gray shales, probably calcareous, especially in the red
layers. At the top the layers weather into rounded masses looking like
concretions ; the lower beds are covered with dSbris, The red layers are
from one foot to 2 feet in thickness, while the green are from IH inches
to 2^ feet. They are rather irregular, however, the colors fading out in
places 45 0
24. Massive, coarse-grained vellow sandstone, with angular fracture breaking
into large square blocks 90 0
25. Greenish argillaceous and sandy shales in laminte of an inch or less thick-
ness 22 0
26. Massive yellow sandstone like that of No. 24 ..^ 11 0
27. Shales like those of No. 25 24 0
28. White, red, and yellow sandy argillaceous and gypsiferous beds 38 4
29. Yellow sandstone resembling that of No. 24 and No. 26, except that it is
not quite so massive, and is gypsiferous 5 0
30. Yellow sandstone, couglomeritic at base, then shaly, and finally massive.. 14 0
31. Argillaceous and sandy shales, greenish, and in fine laminte below, becoming
reddish above 3 0
32. Massive yellow sandstone 6 0
33. Micaceous sandstones and shales, with a band of massive sandstone, 20 feet
thick, in the center. The shaly layers are fossiliferous, containing frag-
ments of bones 100 0
34. Red and greenish sandstone, weathering into rounded masses 10 0
35. Green and red sandstone shales with intermediate bauds of sandstone 46 0
36. Red and yellow mottled, rather massive, sandstone, weathering in rounded
masses 5 0
37. Hard dark-greenish sandstone ? oq q
38. Red irregular sandstone )
39. Soft shaly sandstones with fragments of hones 13 2
40. Massive sandstones 9 10
41. Shaly sandstones with fragments of &one« 57 0
42. Yellow sandstones with bones imbedded 9 0
43. Yellow sandstones, somewhat shaly below but becoming more massive
toward the top, especially in the upper five feet 34 6
44. Argillaceous and sandy shales with fragments of bones 3 0
45. Greenish and reddish sandstones, somewhat argillaceous, weathering in
bowlder-like masses 12 0
46. Massive sandstones 12 0
47. Greenish sandstone, like No. 45 10 0
48. Miissi ve yellow sandstone 50 0
49. Greenish and yellow shaly sandstones, with fragments of hones 150 0
50. Massive yellow sandstones, with imbedded bones, especially abundant in
thelower part 10 0
51. Coarse, soft, gray, shaly sandstones 50 0
56. Massive yellow sandstone 6 0
53. Greenish-gray sandstones, mostly laminated, some of the layers having
mud-markson thesurfaces 100 0
54. Coarse yellow sandstones in massive layers } 75 0
55. Soft gray sandstones with numerous fragments of hones >
56. Soft and hard gray sandstones with interlaminated shales, calcareous and
argillaceous, reaching from the top of layer No. 55 to the base of the
whit-e bloflfs below station 50. The total thickness is about 1, 600 0
67. Alternations of dark-gray indurated clay beds, weathering white, and are-
naceous layers reaching to the summit of station No. 50. Many of these
layers are probably calcareous. Gypsum does not seem to be as abun-
dant as In the lower layers of the section. I did not have time to make
a detailed section. The total thickness is about 1,000 0
Top.
Total thioknesB .6,767 7
158
GEOLOGICAL SURVEY OP THE TERRITORIES.
This section does not give the total thickness of the beds, as it only
reaches to the summit of station 50. The summit of the plateaa
beneath station 48 has about 800 or 900 feet more of beds similar to
those given in the section above, under Ko. 57. Even this thickness,
about 7,670 feet in all, may not represent the entire original thickness,
for we cannot at presents tell the exact amount of erosion preceding the
pouring out of the basaltic covering of the two plateaus.
The following section is summarized from Professor Cope's report
in the Annual Report of the United States Geological Survey for 1873,
pp. 436, 437.
Wahsatch formation '{Oreen River group).
Thiokneis
in feet
1. Asb-colored banks, ^ith bones of a mammal allied to tbe Bridger Hyapsodm^
or Hyracotherium of the Eocene of Europe and a number of Palvdina-Mke
shells, followed by light ash-colored beds exposed in banks, with bones of
Green River vertebrata. Near the top is a thin bed of lignite 140
3. White bluffs, terminating in a high escarpment i
3. Thin bed of buff clay and sand-rock, with numerous shells and scattered > 100
teeth and scales of fishes .' i S
4. White bluffs..... 100
5. Brilliantly colored strata extending in horizontal bands. Ihey are brilliant
cherry red, white, true purple, with a bloom shade, yellow, and pea-green.
The lower portions are bright red and contain remains of Emys euthnetuSj
Cope, and some borings of a worm 400-f>00
6. Muddy-yellow clays and slate-rocks 200
7. White or ashen beds, with decayed remains of mammals and turtles, also
buff sandstones 50
Bridger group,
8. Mammoth buttes ; sediments with numerous mammalian remains 1, GOO
Total thickness 2,090
The resemblance of the beds I haye given in section No. 19 will be
seen at a glance. Tbe following table of comparison will give tbe
relatioDS of the two sections :
SectioD No. 19, A. C. Peale.
Layers Nos. 1 to 55,iDcIaaive
La^^'ers Nos. 55 to 57 inclusive, with tho 900
feet of additional beds not given in tho
section
Total
Thick-
ness.
4,170
3,500
7,070
Prof. £ D. Cope*s section.
Thick,
oesa.
WahMatoh formation, (Nos. 1 to 7, inclasivis) 1, 090
Bridger group, (So. 8)
Total.
1,000
S.090
It will be noticed that the thickness on Plateau Greek is mach greater
than that given in Professor Cope's section. Comparing section Na
19 with the descriptions given in the tables (page) we see the similar-
ity in composition of the strata. The fossils obtained could not be iMW-
itively identified as to whether they were from the Green Itiver or
Bridger groups.
The bones from the layers, Nos. 33, 39, 41, 44, 49, 50 and 55, of the
section No. 19 were submitted to Prof. E. D. Cope for examination. He
says they are " undoubtedly Eocene (Bridger or Green River). I find
species ofrejitiles and fishes; the former CrocodilvSy Emys, and Trionyx;
the latter PappichthyaJ'
miB.] GEOLOGY— GREEN BIVEE BEDS. 159
Tlie beds given in the lower part of the section are probably of the
same horizon as the Green Eiver groap, as I have shown in the table,
while those above represent the Bridger group. It is impossible at
present to tell any more definitely the line that separates them.
The following is the description given by Dr. Hayden* of the Green
River gronp, as exposed in the valley of Green Biver : *' The lauiiuated
caleareons shales gradually pass down into yellow gray and brown in-
durated clays, sands, and sandstones, until the well-defined coal-strata
are exposed without the least appearance of discordancy." In other
portions of the report for 1870, he gives descriptions of the Green liiver
group, and speaks of their being worn into towers and other picturesque
forms. Prof. Theo. B. Comstockf gives the following description:
<'The Green River beds are mainly composed of a series of shales, marls,
and harder calcareous strata." *' The texture of the different beds is
quite variable, but in general the streams which have cut their chan-
nels through them are walled by nearly vertical cliffs, and the buttes
and benches for the most part have quite precipitous sides. Numerous
joints occur in many of the strata, particularly in the more compact
kinds, and fine examples of concretionary structure or weathering are
not rare. The tendency of the thick beds of marly sandstone on the
banks of Green River, at the crossing, to weather spheroidally is very
noticeable, and this is repeated in various degrees in the argillaceous and
calcareous rocks as well." In regard to the Bridger group he says,| <*The
beds of the Bridger group, as a whole, are readily distinguishable from
those of the Green River group, being mainly composed of dull-colored
indurated clays and arenaceous layers of considerable thickness, the
latter usually brownish, or dull yellow or gray, often with more or less of a
concretionary structure." Dr. Hayden (see Report of 1870) gives the
same general description. I have quoted these descriptions to show the
resemblance of the strata given in the section made on Plateau Creek to
the strata found farther north. A comparison shows the same general
characters, even to the spheroidal weathering of some of the layers.
Although the beds included under layer No. 57 of the section correspond
to the description quoted above of the Bridger group, their identity is
by no means certain. Another season I hope to obtain more evidence
on the question. These beds form the cliffs immediately beneath the
plateau of station 48, and are prominent from a great distance, on
account of their white color. They also outcrop in the cliff's on the
north side of the Grand opposite the plateau and extend far to the north-
ward. They are also seen far to the westward and southwestward, be-
tween the Colorado and Little Colorado or Chiquito Rivers. In this
region they are thus referred to by Professor Newberry :§ " Some miles
north of camp 96 {situated about latitude 30^, longitude 110^ 45') a mesa
wall rises to a height which we estimated at something like twelve
hundred feet. It occupies 30^ of the horizon in that direction, and shows
bold, nearly perpendicular faces both in profile and in front. These are
imre white in color and reflect the sunlight like sun." '^ Rising, as it does,
80 distinctly irom the mesa of Lower Cretaceous, but two formations are
left in the series of which it could be composed, Upi>er Cretaceons and
Tertiary." These bluffs are probably a portion of the same strata that
form the bluffs on the Grand and beneath the plateau of station 48.
Professor Newberry did not have an opportunity to examine them, but
• Report U. 8. Geol. Survey, 1870, paffe 71.
t Report upon Reconnaissance of Northwestern Wyominf^, 1873, pages 123, 124.
t Report upon Reeonnaissance of Northwestern Wyoming, 1873, page 127.
t Ives's Colorado Exploring Expedition, Geological Report, page S7.
160 GEOLOGICAL SURVEY OF THE TERRITORIES.
considered tbem to be of Upper Cretaoeoas rather than Tertiary age.
He says, ^^ There are some reasons, however, why we shoald sospeet
this white mesa to be Upper Oretaceoas rather than Tertiary, and these
are, first, that all the Tertiary rocks of the Bocky Mountain country, as
far as they have been examined, are of fresh-water or estuary ori^n,
have been usually deposited in basins of less extent and depth than
would be indicated by this great plateau, which has evidently been
greatly reduced in dimensions by the erosion it has suffered ; second,
tlie materials composing the Tertiary strata found on the great cental
plateau are generally soft, and yield readily to the action of the elements,
presenting rounded and unbroken outlines or pinnacles and deeply chan-
ueled surfaces, the results of erosion. On the contrary, the Upt^er Cre-
taceous strata, as they appear in several points on our route, holding
pre<*i8ely the relative position of the white mesa to the Lower Creta-
ceous sandstones, consist of a series of shales and limestones which,
though dark internally, weather to an almost chalky whiteness, and yet
are as resistant to atmospheric erosion as any other sedimentary rocks.
Judging from the view we had of it, we regarded the white mesa as
continuous with the white mesa bordering the Colorado, which bas
about the same altitude. If so, the strata composing it must occupy a
very large area north and west of our camp 96, one almost too large to
accord with the supi>08ition that it is of Tertiary age."
My reasons for referring the strata of section No. 19 to the Tertiary
are, first, the finding of vertebrate organic remains identified by Profes-
sor Cope as of Eocene age ; and, second, the lichological identity to the
beds farther north, in which Marsh, Cope, and Leidy have found so
many vertebrate remains identified by them as of Eocene age.
As already noticed in the preceding chapter, the strata included in
the Upper Cretaceous weather very white, although they do not show
so prominently as the upper portion of those given in section No. 19.
It is impossible at present to define the exact limits of the basin in
which these layers were deposited. As mentioned in preceding parts of
this report, the Sawatch range was probably partially above water in
Cretaceous and Pre-Cretaceous times. It probably formed a part of
the eastern shore of the ancient lake, although all traces of the beds
along its western flanks have been entirely removed. To the northward
it was probably connected with the Green River Basin. Prof. T. B.
Comstock,* speaking of the Green Kiver group, says, " There are indi-
cations that its eastern boundary was outside of the present limits of
the Green River Basin, and there is no room for doubt that the Uintah
Mountains and the Wasatch chain, then as now, towered above its sur-
face. Northward it is equally clear that the Wind River range formed
the shore of the great lake, with probably more or less of gently sloping
border, during a portion of the era of Lower Eocene deposition." Be-
fore we can decide definitely as to the connection of the strata of the
Green River Basin with those noted between the Grand and Gunnison
Rivers, the country north of the Grand will have to be examined.
What the sontherii and southwestern limits of the lake were, it is im-
possible to say at present. Enough has been said to prove its vast
extent in that direction. The investigations of the next season's work
will probably throw considerable light ui>on the sulyect.
Professor Marsh discovered evidence of a basin south of the Uintah
Mountains, aboUt the mouth of the White River. This is probably the
direct extension of the basin 1 have described. Professor Marsh thinks
* Report upon the recoDDaiesaDCO of Northwestern Wyoming, p. 123.
KAULl OEOLOeY — ^POST-TEETIABY AND RECENT. 161
that although syBcfaronotis with the Green River Basin, that the lakea
were conneeted only as oar great lakes are at the present day, by uav-
row straits.
POST-TEBTIABY AND BEGENT.
OUiciaL
In the Sawntch range, as was fnlly detailed in the reports for 1873^
there is abundant evidence of glacial action. The moraines in tbf
eaiions at the head of Eagle River have been already described. It is
impossible, with the present limited amonnt of datia, to define whM
were the limits of the glaciers. It is probable they were more widely
distributed than has been generally supposed. It is possible that a
Racier once covered the plateau of station 48, and the one to the south.
The erosion on these plateaus could scarcely have been effected by any
ether agency. There are several lakes on the surfkce which may have
had their origin in glacial action.
Farther north Mr. Marvine found evidences of gladation on similar
plateaus, capped with basaltic lava. They were, he thinks, at a higher
level, and when ho descended, the traces ceased. The Roches^Moa*
tODn^4)8 forms were very prominent.
Terraces J etc.
Eagle Biver, — ^In the valley of the Eagle, above the second cafion, ex*
tending almost to the mouth of the Piney, are terraces cut in drift.
Whether this drift is stratified or unstratified I am unable to say. It
is, I think, in part at least, of glacial origin. The terraces here are
about 100 feet high. Below the canon there are beautiful terraces, as
shown in section D, Plate III. These are comparatively recent. The
soft character of the strata in the valley renders them easily eroded,
and even at the present time an immense amount of material is carried
down the nver every spring. Alluvial material occurs at various points
along the course of the river, especially above the second caiion, where
the river has some lake- like expansions surrounded by beautiful
meadows.
Grand River, — A great portion of the Orand River is a caHon, but
below the mouth of Roaring Fork, especially near the plateau of station
48, there are terraces. We did not have time to visit this part of the
river, and simply noted them from a distance. The alluvial bottoms
are very limited in extent.
OiinHison Biver. — ^The valleys of the Gunnison, its North Fork, and
their tributaries are terraced in a beautiful manner. All the drift is
probably of local origin. The terraces are cut mainly in the soft shales
of Upper Cretaceous age, which have been treated of in the previous
ehapter. There are scattered patches of alluvial material. These areas
have already been described, and description here would be a repetition.
Eroeian.
■
The valleys of nearly all the streams in the district are simply erosive,
although a number were i)erhaps determined in the^r present course by
breaks in the strata, the result of folding. It would be impossible even to
estimate the enormous amount of erosion to which the strata west of the
continental divide, in our district, have been subjected since the begin-
ning of Tertiary time. The amount of erosion during the Tertiary time
was enormous. It was sufficient to form beds thousands of feet in thick-
11 H
162 GEOLOGICAL SURVET OF THE TEBRITOKIB&
iiess. In section No. 19 of Tertiary strata we have seen that there are
over 7,000 feet of beds. A large part of their ingredients was doabtless
derived from the Sawatch range. Over the mass of the Elk Moantains,
the Cretaceous, with underlying strata, have been removed, to a great
extent, leaving only on the edges remnants of the Cretaceons. On the
western flank of the Sawatch we see no Cretaceous. This will give ns
some idea of the enormons denudation that has been e£fected. A large
portion of this denudation was doubtless the result of glacial action.
The erosion going on at the present time is by no means inconsider-
able in amount. The high water dnring the spring months carries
down a vast qaantity of material. Dunng the rainy seasons the rain
comes in frequent showers, which, although of short duration, are very
violent, and wash down immense quantities of material, cutting deep
gullies into the blnffs. The softness of the beds on Eagle River, on
Grand Biver below Ebaring Fork, and on the North Fork of the Gun-
nison, renders them very susceptible to aqueous influences. In the
mountains, the alternate freezing and thawing of the snow-banks, in the
spring and summer, has considerable influence on the erosion. The
alteration in the level of the streams is often very perceptible.
Another agent of erosion has been pointed out by G. K. Gilbert, in a
paper read before the American Association tor the Advancement of
Science, in 1874, viz, that caused by the action of sand carried down
the streams on the rocks through which they flow. The erosion effected
in this way is very considerable, especially where the beds of the streams
are in solid rock. Our district was so broken by hills that the action
of wind in eroding the strata is not so noticeable as in more level coun-
tries.
PI
I
CHAPTER VIIL
EBUPnVE BOCKS— TBAGHTTES—TBAGHOBHBITES--BASALT.
I separate the volcanic areas of the district into three divisioDS,
according to the cliaracter of the rocks coveriug them: flrst, the porphy-
ritic trachyte forming the group of mountains marking the western or
fiOQthwesteru termination of the Elk Mountains in the southeastern
portion of the district; second, the trachytic areas (mostly rhyolitio
underlaid by breccia) which form a large part of the southern portion ;
third, the basaltic areas that prevail in the northern part.
Tbe rocks of the second division correspond to the ^'Trachorheites''
of Dr. Endlich, and in fact are the northern and western extension of
tbose rocks described by him in the report for 1873 under section c*
With the exception of the first division, the volcanic rocks form the
tops of phkteaus which have be«n much modified by erosion. These
plateaus are generally covered with a luxuriant growth of grass and
scattered groves of cottonwoods.
Tbe volcanic rocks of the first division form beautiful isolated mount-
ain masses, surrounded with sandstones of Cretaceous age.
The rocks of the third division are probably of most recent age,
although it is difficult to say definitely that they are more modern than
tbe rhyolitic rocks in the southern part of the district. The latter pre-
vail largely in the district assigned to Dr. Endlich, and he probably
Kcnred more evidence as. to their age than I was able to.
POBPHYBITIO TBAOHYTES.
Although the rocks that I shall describe under this head differ con-
Nderably from each other, they have the same general constitution.
Tbey contain the same minerals, and are generally of lightgra> colors,
lirith crystals of feldspar porphyritically imbedded in the mass with
borublende and occasionally mica. They resemble the rocks found
throughout the Elk Mountains in 1873, especially those found at Gothlo
Mouutaiu and the various dikes found penetrating the sedimentary
formations. iSome of the more compact varieties have a granitic appear-
ance, reminding one of the rocks forming the central masses in the main
mass of the Elk Mountains.
The physical featuresof the country in which these mountains are have
been fully described in previous portions of the report, and I therefbre
Bimply refer to them here.
The isolated character of the i>eak8 is well shown in Plate XI. a, b,
and e represent some of the trachytic peaks, which stand like huge
monuments in the midst of the Cretaceous sandstones which are seen
outcropping in the bluff in the foreground of the picture. At d and e
h shown a dike of trachyte, which once formed one continuous masa.
* Bepon U. 8. GKiol. Survey 1873, page 343.
163
164 GEOLOGICAL SURYET OF THE TEBKITOBIES.
It is scarcely to be doubted that all these mountains are eraptive in
their origin. The evidence pointing to this fact will be referred to as
we proceed. The sandstones surrounding them seem to have been but
little disturbed by the thrusting-up of these masses. It is difficult to
get at the line of junction between the trachyte and the sandstone, as
the slopes on the mountains are very steep and the bases are entirely
concealed by the mass of dibris washed down. It is probable, how-
ever, that the ends of the sandstones would be found slightly tipped up.
On Anthracite Greek, on the north edge of Mount Marcellina, the sand-
stones are tipped up and penetrated with dikes, as shown in Plate
XII. On the northern side of the area, marked A, on the map G, the
sandstones are tipped up, dipping to the northward at an angle of 20^
to 250. It is a curious fact that these western terminations of the Elk
Mountains should all be trachytic, while in the main mass of the Elk
Mountains the granitic character should predominate. In the dikes,
however, the rock was always trachyte. Proceeding westward, also,
trachyte became more abundant. In the region I have under con-
sideration at present the varieties of rock that most resembled granite
were found in the eastern portion. The dikes always gave the best
typical specimens of trachyte. Some of the sj^ecimens are rhyolitic
I only refer to these facts to show the analogy between the trachytes
and the eruptive granite of the Elk Mountains. Until these rocks are
all subjected to a dose microscopic and chemical analysis and the region
in which they are found examined in detail, all opinions must, to a cer-
tain extent, be conjectural. The Elk Mountain region presents one of
the moat interesting fields of study, and one which will yield more
material for the study of eruptive granites than any other on our conti-
nent.
I will take up these areas in the order in which they are lettered on
the accompanying map (G), which gives a much better idea of the out-
line of each than could be given in words.
The eastern groups are those which, in Lieutenant Buffner's report,*
are called the Philosophers' Monuments.
A. — In ascending Ohio Greek, the hill on which station 30 is located
forms a prominent feature of the landscape. It is sugar-loaf in form,
and rises over three thousand feet above the level of the valley of Ohio
Greek. Its slopes are steep, and at the base is an accumulation of rocks
that have been washed down its sides. The rock is a porphyritic
trachyte. There is a rather compact matrix, inclosing white crystals
of feldspar, free quartz, and small crystals of black mica. The mass
north of station 30 is broad-topped, and composed of the same kind of
rock. East of station 30 is another mass, not shown on the map. It
was not visited, but is probably similar to that of station 30. The west-
ern part of the area, marked A' on the map, is a ridge, with numerous
sharp points. The pass from Ohio Greek to the head of Anthracite Greek,
is at the eastern end of this ridge, at the point b on the map. This pass
is 1,800 feet below the summits of the ridge. I am in doubt whether or
not this area is separated from the mass of station 30, marked A. I have
provisionally connected them on the map. At the western end I am also
I doubtful, as I have never been on the saddle that separates it from the
'area E. This saddle seems to be comparatively low, as seen from the
surrounding country, and I think it probable that the Gretaceous sand-
stones connect across it. The dotted lines indicate the doubtful part.
On the north side there are Gretaceous sandstones dipping to the north,
* Report of a KeooauiasNioe in the Ute Country, page 40.
I-
^
12
(X
' * _ •«
*
' 0' • t
•o
I
>52
•^
rziLB.] GEOLOGY — PORPHYRITIC TRACHYTES. 165
at an angle of 20^ to 25<^. It is in these sandstones that the anthracite
eoal occnrs, at the point marked m on the map. On the southern side
there are also sandstones, bnt, as far as I observed, they are horizon-
Ul. Towards the west end of the ridge, resting on these sandstones, is
a mass of breccia, which seems to abut against the trachyte. The line
on the map indicates this breccia. A specimen of trachyte from the
eastern end of the ridge has a rhyolitic appearance. It is light-gray in
color and coutaiuH a great deal of fiee quartz. The matrix is rather
coarse, and contains large crystals of glassy feldspar and small besag-
onal crystals of a brownish-black mica and a few small needles of horu**
blende.
Above the coal-bed mentioned as occcnrring on the north side of this
area there is a layer of trachyte in the shales and sandstones. It
resembles the rock just described in appearance and construction, being
perhaps'a little rougher and having the hornblende in greater quantity.
The crystals of feldspar are not so large. The free quartz has the
appearance of pebbles, the edgea being rounded, probably the result of
heat.
B. — Station 32 is the mountain named Mount Bichard Owen by Lieu*
tenant Bnffner.* He says, ^^ Mount Richard Owen has two peaks, the
Dortberu of which is the higher, of dusty-red rock, probably ferruginous
qaartz, or perhaps trachyte." The mass of which station 32 is only a
portion, is composed of Cretaceous shales and sandstones intersected
and metamorphosed by numerous dikes, of which the principal ones are
shown on the map. To accurately define all the dikes in this region
vill reqnire a very close and detailed survey. Station 32 seems to be
a center for them. In the ridge southeast of the station there is a layer
of trachyte between layers of sandstone. The section in which this
occura was given in a preceding chapter. This rock is rather moro
compact and finer textured than the trachytes I have hitherto described.
Tbe porphyritie character is not so decided. It is of a light greenish
color, and Wms to be slightly arenaceous, as though it had taken from
tbe surrounding rocks a portion of its sandy material. It is perfectly
cooformable with the sedimentary rocks, and, under other circumstances,
might be taken for a contemporaneous flow. It presents a square, mass-
ive edge on the bluff, as shown at C in Plate X. The dike, marked a b
on the map, is also shown on this ridge cutting across it alm^ost at right
angles to its strike. It is about 300 feet in width on the ridge and
iaeliues slightly to the northeast. At right angles to it is a narrow
seam of quartz, inclining west at an angle of 85^. This seam could be
distinctly traced for several miles on the ridge. I was unable to trace
the eastern extension of this dike to its extreme limit. The rock of this
(like is a greenish-gray trachyte, rough in texture and containing a
large number of feldspathic crystals.
Crossiug the same ridge a little farther north is another dike, the one
marked efou tbe map. Plate Xlil shows the appearance of this dike
»8 seen on the face of the bluff, aaa representing different portions of
it intersecting the sandstones bbhb. The rock in this dike differs
greatly from the others. It has a very compact, fine-textured, dark-
greenish matrix, in which are a few small crystals of feldspar.
They are more conspicuous on the weathered surfaces. Besides the
feldspar there are particles of free quartz. The specific gravity of this
lock is greater than that of those from the other dikes. The dike c d
of the map forms a very prominent ridge leading down fhm station 32
^ |-ri¥ii I 1- I --r--MB- 1 — ■- - — - n - n T
* Beport of KeconiialManco in the Ute Conntry, page 40.
166 GEOLOGICAL SURVEY OF THE TEBBITOBIES.
to AntLracite Greek. Its bardDess has preserved it while tbe sorroaod-
iDg rocks have been removed. Its summit presents a ragged edge, spire-
like processes rising from it. The rock is very mach like that of Meant
Marcellina, and that of areas described under A and A'. The dike g h
has a course almost at right angles to tbe one described. 1 was unable
to visit it, but am inclined to think it a continuation of the one marked
a b. Other dikes in this region are shown, but were not visited. They
by no means represent all the dikes that are to be found, but merely tbe
principal ones. The mass of mountains north and east of station 32
contains many more that we were unable to define.
C — ^The center of this area is Mount Marcellina, a steep mountain, the
general shape of which is sugar loaf. It is shown at a in Plate XL
This is probably the mountain to which Lieutenant Kuffner gave the
name of Mount Huxley,* as it answers the description. On the map
accompanying his report, however. Mount Huxley is marked as being od
the opposite side of the creek. It being, therefore, somewhat doubtful,
we have used the name Marcellina applied to it by prospectors that we
met in this region. The slopes are very steep, and the base surrounded
by a mass of dShrU. The sides are weathered into conical, spire-like
forms which stand out in bold "relief, especially on the western and
southern sides. It is 11,324 feet above sea-level, and about 3,000 feet
above the top of the sandstones that form the surface between it and
the area marked D on the map. It is over 4,500 feet above the level of
Anthracite Greek, on the northwest side. The trachyte of Marcellina is
very fine-grained, resembling closely the eruptive granites of the Elk
Mountains. On the northwest side of the mountain the Cretaceous
layers are tipped up, dipping to the northwest 15c> to 2(P. This is the
only point at which any disturbance of the strata around the mountaiD
could be seen. Here also they are penetrated by dikes of the same
material of which the main mass is composed. It was perhaps more
porphyritic. Plate XII represents three of these dikes on the south-
west side of the creek. On the opposite side there is a much larger
mass of this rock resting on the sandstones. I think it probable that
t'ae trachyte extends from Marcellina to the north side of Anthracite
Creek. Whether it extends to the westward connecting with C I am
not so certain. I have indicated the intermediate portion by dotted
lines. We did not have time to follow Anthracite Creek throughout
its entire length.
D. — ^This area is the second in size, and comprehends 25 or 30 square
miles. It consists of a number of sharp peaks connected by sharp
ridges bounding amphitheaters in which rise streams tributary to Kock
Creek on the north and east, and on the south and west flowing to tbe
iN'orth Fork of tbe Gunnison. The western side of this mass is very
steep, the angle of the slope being about 50o. The summits are from
2,000 to 2,500 feet above the general level surrounding the mass. This
western side is not broken up by gullies, it preserves a uniform wall-
like surface for nearly three miles. Tbe amphitheaters thait we have
referred to are found on the sontbern and eastern sides, the majority of
the drainage being into liock Creek. The eastern side is ther^ore most
irregular and shows most markedly the effects of erosion. Hock Creek,
opposite station 33, before it bends to the northward is 5,000 feet below
the summits of the peaks. The rock of station 33 is similar to that of
Marcellina, the only difterence being that the component parts in the
former are much coarser.
At D' and D'^ there are two areas whose limits I am unable to define
^ Report of BeoooDaissanoe in Ute Coantry, p. 41.
N
I
I
IhrphfHlic (TTTT^
— t
ntOTaUTMOOMlMttl Wl
0 e.
' " , . ' '■
MAI* J GEOLOGY — ^^ORPHYRITIC TRACHYTES. 167
with exactness. Between D and D^ there are Cretaceons rocks. Treas-
ury Mouutaiu forms the center of the second area. The Cretaceous
rocks in this region have been lifted up and so broken, that the lines
of ontcrop cannot be distinctly seen from a distance. For more detailed
information in regard .to the rocks here, the reader is referred to Mr.
HoImes^s report.
E. — Only the western end of this area was visited. A view of it is
Been in Plate XI, at b and c. The area E' is seen at d, and E" at e. The
two latter are evidently parts of the same dike; a branch of the creek
separates them. At E^^ the trachytlc simply caps the ridge, forming
a small isolated patch. This dike was once evidently connected with
the trachyte east of station 34 (the area F). The dike d in the illi^s-
tration is evidently connected with the mass b. Th6 rock from the
dike dififers slightly from that already described, the mica not being so
predominant. It also contains more hornblende. It is of a verj" light
gray color, very compact and fine-grained.
F. — ^This is the most irregular, and by far the largest of the trachy tic
areas. It includes 50 or GO square miles. Our most eastern station in
this area was station 34. In ascending the ridge towards the station,
there was noticed an indistinct lamination in the trachyte; some of the
beds have calcite. There seems to be an alternation of hard and sof&
layers, rocks from the latter weathering with ronnded edges. The trachyte
is more vesicular than any yet described; the crystals of feldspar
are clearer and have more of a glassy appearance. The rock is gener-
ally of a dull-gray color. The weathering of the mass, of which station
34 is the center, is very different from that of Marcellina, and of the
ndge forming the area E. The mountains here are more massive, and
the creeks draining them head in amphitheaters, separated from each
other by long sloping spurs which have very steep ends. To the north-
east they descend to the top of a mesa of sandstones. This mesa on
the opposite side of the creek is shown in the forgeround of the picture
io Plate XL
On the east the descent to the level of the creek is very steep. There
are remnants of Cretaceous shales, with coal still resting against the
eDds of the S])nrs«
The arm that extends to the southward, west of station 36, rests
against a mass of breccia, which will be described with the next division,
of the eruptive rocks. The northern edge of this breccia is indicated
by a dotted line. In this southern area there are four or five prominent
}>eak8, none of which we visited.
Between the southern arm and the southern prolongation of the
western arm around station 37 is an irregular area of Cretaceous, which
has been fully described in a previous chapter. The eruption of the
trachyte seems to have caught these rocks and tipped them up in all
directions. They seem also to have been much metamorphosed.
In the western arm, stations 38 and 39, are the principal peaks. In
the arm connecting this part of the area with that to the eastward there
are several peaks equally high. Station 38, as viewed from the west,
is a sharp, conical peak, rising very steeply for 1,800 or 2,000 feet, and
from that point sloping gradually towards Smith's Fork. Fig. 1, Plate
VII, gives a section from the station westward. Station 39 is also sharp,
and also shows very prominently from the north. The rock of both
mountains is the same. Numerous white crystals of feldspar and a few
crystals of hornblende are imbedded in a gray matrix. The country
around both stations is comparatively low and filled with soft shales of
the Up[>er Cretaceous layers which form low butte-like hilhi. Seen from
168 GEOLOGICAL SURVEY OF THE TERBITOBIES.
the sammits of the peaks they seem merely irregularities io the sarface^
Station 38 is 10,634 feet above sea-level. It is the last peak of the
Elk Moantaios to the west, and from its summit one can see the dim
outline of the Sierra la Sal Mountains, 100 miles farther west. Station
39 is higher, having an elevation of 11,337.
Cr» — This area consists of a double-topped hill of trachyte, rising
about 1,000 feet above the cretaceous rocks that surround it. It is well
wooded to its summit, which is bro^d. The slopes are not very steep.
The North Fork of Smith's Fork curves around its northern end. The
trachyte composing it presents no features different from those of the
rocks already described.
H* — Opposite this double-topped mountain, which we called Saddle
Mountain while in the field, is a trachyte x>oint rising between 300 and
400 feet above the level of the creek, standing like a finger in the midst
of the Cretaceous rocks.
K. — This is the last trachytic area to the westward. The bill in
which' it is shown is low and rounded, being only 1,800 feet above
the level of Smith's Fork. The face toward Smith's Fork shows the
trachyte best. It is of a light-gray color and porphyritic It does
not differ materially from that of station 38. East and north there are
Oretaceous shales, and on a low hill back of it there is a dike of similar
rock lying at the base. This is on the layer marked No. 1, in section
16, given in chapter VI. The eruptive force seems to have been dying
out to the westward, and the last evidence we have of its action is in
the canon of the south branch of Smith's Fork, where the bending of
the No. 1 Cretaceous caused a break, which gave origin to the canon.
In the consideration of the areas just described it will have been no-
ticed that there were numerous points at which the intrusive character
of the trachyte was not to be doubted, as near station 34 and near
Mount Marcellina. These rocks are the same that are seen in the large
areas, and if intrusive in one place are probably so in the others. The
elevation of these mountains is Post-Cretaceous, and probably of more
recent date than the rhyolitic flow from the south, for the northern edge
adjoining this area is tipped up, where the trachyte has not been re-
moved, and, where it has, the underlying breccia forms the summits of
the mountains, its level being much higher there than along the Gunni-
son Biver.
TBACnOBHBITES.
Under this head I will describe the rocks of the mesa like country
extending along the Gunnison, on both sides, as far as the Grand
Canon. The accompanying map (map D) will give the extent and dis-
tribution of the rocks comprehended. Their character and order of
superposition will be given in detail as I proceed. 1 he source of the
flow is to the southward in Dr. Endlich's district, where there is a much
greater thickness of the rocks, those exposed on the Gunnison being
merely the overlying edges of the upper layers, those underneath not hav-
ing spread so far to the north. East of Ohio Creek there are two mesa-
like summits crowning the broad ridge between Ohio Creek and East
Biver. These mesas are trachytic, and seem to rest immediately upon
beds of Cretaceous age. I do not think there is any breccia beneath, as
there is farther west. The general level of the mesas would seem to
indicate that they are remnants of the layer that forms the mesas north
of the Gunnison. The hills west of Ohio Creek are composed mainly
of breccia, the trachytic capping having been removed. The soft
beds have been eroded in the most fantastic fashion. The bnccia is
(h
• /
/
' f '^ •- n
Plate XIV.
G
K
I
^
Tlffl.SecUorvN. ^
Fi^. 2 Section, O.
J*fO 3 .SecUarv P.
, o
.■Ja;.r
• '• ft
. •• Xf
« «
Fcy^i:iccti(n R
WALR.) GEOLOGY — ^TEACHOEnEITES — GUNNISON EIVEE. 169
stratified, and tbere are huge castle-like forins, abrupt walls, and spires
and towers. Station 31 is situated in the midst of a mass of hills of
this material, their summits being generally broad and rounded. The
thickness of the breccia at station 31 is about 3,000 feet. These hills
slope toward the Gunnison in long, gentle spurs. The breccia north of
station 31 rests against the edge of the hills of x>orphyritic trachyte,
already described. It rests for the most part on Cretaceous sandstones.
The line of Junction is seen on the west branch of Ohio Greek and on
the Ounnison at various points. It is probable that in the center there
may be shales between the sandstones and the breccia, as at station 73,
oil the Gunnison. The valley of the Gunnison, on the north side from
Ohio Creek as far as station 71, has been subjected to considerable erosion,
and the breccia forms the basis of the hills. It probably rests partly on
the schists, with an occasional patch of sandstone between, as indicated
by an outcrop in the bluff opposite the mouth of Cochetopa Creek.
Fig. 4, Plate XIV, represents a section across the Gunnison, in the
meadow below the mouth of the creek. Fig. 3, on the same plate, is
a section through station 71. Here the sandstones appear and the
breccia is capped with a white rhyolitic rock, which is probably under-
laid by obsidian and tuffa, as we see farther down the river. Under
station 71 the line of junction is concealed. West of the station, below
the canon which the river cuts in the schists, there is a steep dip of the
sandstones to the west or southwest, which is the reason tliey do not
oatcrop in the section in Fig. 2, which is made below th^ ca&on. Bor-
dering the valley in which this section is made, on the north side, are a
namber of buttes capped with obsidian and trachyte. Back of them the
mesas extend toward the hills to the northward. These mesas are
exposed on both sides of the Gunnison. At station 73 I made the fol-
lowing section of the volcanic layer :
Section No. ZO^Gunniaon Siver, near station 73.
XJllckBMS.
JBaM. Foet.
4h Breccia 400
'2, Light pinkish-white tafa
«
2. Light piokish-white tafa ^
3. Gray lamioated trachyte I mq
4. Hard obsidian i)orphyry f
.5. Soft sphemlitio and porpbyritic obsidian J *
#)6. Pnrple vesioalar rbyolite 50
^ 1 7. Blnish-gray rhyolite 30
Top.
Total 520
This section goes as far as the top of the bluff, but as we go back
there is a greater thickness, and probably a repetition of the upper por-
tion of the section, that is from the obsidian upward. The letters in
the section above correspond to the letters in Fig. 1, Plate XIV. As
the rocks of this section are typical of the rocks in these mesas, I will
describe them more in detail. The breccia I will pass by for the pres-
ent The tufa, which rests immediately upon it, is almost white in color,
and appears to be made up mainly of feldspathic material, with parti-
cles of quartz and mica interspersed. It is soft and very fine in texture,
having a sandy feel when crushed in the fingers. Above station 73 this 4
toff is about five feet thick. Layer No. 3 is a dull, purplish-gray rock,
in which there are numerous particles of quartz and obsidian, with crys-
tals of sauidine porphyritically imbedded. There are also a few crys-
tals of black mica. Under the glass this rock has a vitreous appear-
ance. It is probably rhyolitic. It is from two to four feet thick. Layer
^0. 4 is very hard, and breaks into square blocks, with very smooth.
170 GEOLOGICAL SUBVEY OF THE TEBRITOBIES.
regular faces. There are nameroas crystals of sanidine in the obsidian.
As we ascend, the bed becomes softer, and besides sanidine contains
small spheralitio masses, which are generally aboat the size of a pin-
bead. In some places, however, they are an inch or two in diameter,
and when broken open the cavities in them are found coated with
Hyalite. This sphernlitic obsidian is exactly like that fonnd b^^ us io the
Yellowstone National Park,* and a description of one would answer for
the other. Layer No. 6, iu the section given above, is a compact jaspery-
looking rock, slabs of which ring under blows of the hammer. In the
cry pto-cry stall ine paste are crystals of sanidine, bronze mica, free qnartz
in abundance, and occasionally a pebble of what has the appearance of
having been tufa inclosed and metamorphosed. This rhyolite is vesicular,
the cavities being lined with blue chalcedony. These cavities are most
abundant in the lower part. The description of this rock answers for
the layer wherever it is shown along the Gunnison, the only difference
being in the color, which at station 73 is a pnrpliHh-brown. At station
77 it is more of a gray. The geodes of chalcedony are very abundant
in the latter place. Layer No. 7 breaks into slab-like musses which
weather white. They ring under the hammer like the layer below.
Just above it are indications of a tufa, resembling that above the
breccia. It seems to be of a reddish color. Along the second creek
west of station 73 the trachytic capping has been removed, and the
breccia forms the basis for a considerable distance up the creek,
the mesa-form disappearing with the removal of the trachyte. The
creek west of stations 77 and 78 forms the present western boundary
of this trachytic area. At the head of the creek, as seen from station 79,
the trachyte is tipped up, dipping toward the south or southeast at an
angle of 10^ to 15^. This is also the general direction of tbe sloi>e of the
mesas. Station 79 was located on a point capped with a remnant of
the lower part of the trachyte, below which is the breccia. It is im-
possible to tell at present how far west this flow originally extended.
The breccia which we have referred to so often in the present chap-
ter is generally of a dark-gray color in the matrix. The included masses
are of all sizes, and generally angular. The greatest variety is seen
near station 31. I have already spoken of the stratified- character at
this point, which seems to indicate its deposition in water.
The upper layers seem to be lighter-colored and to have the included
smaller, masses. Farther down there is a dark band, below which the
included rocks are in large masses. These layers are variegated, red,
green, yellow, and gray. Between the layers are bands resembling a
hard sandstone and also tufaceous layers. The included masses are, I
think, all trachytic. The tufaceous layers are pink and ash colored,
and contain conspicuously black mica and minute crystals of hornblende.
Preceding the deposition of this breccia, there was considcnible
erosion, as is indicated by comparing the underlying rocks at station 73
with those under station 79. In the former place there are only a few
feet of shales between the Dakota group and the bottom of the breccia,
while at station 79 there must be at least 1,000 feet, and tbere is probably
more farther back. On the Gunnison, also, as seen by the sections in Plate
XIV, there is abundant evidence of such erosion. The drainage bad
probably the same general direction as at present. It is also probable
that there was an interval between the deposition of the brei*.eia and
the flow of the rhyolitic rocks, during which there may have bet^n
some erosion of the breccia. It varies grciitly in thickness. At stalion
31 it is 3,000 feet, while on the Gunnison, at station 73, it is only 400 /eet.
* Beport U. S. Geol. Survey, 1872, page 131.
%
•4
%
Library. ■
«k.
nkis.] GEOLOGY — BASALT — EAGLE BIVEE. 471
I have already stated that tbe origin of this trachyte and breccia is
ID Dr. Endlich'8 district, south of tbe Gunnison. Since it was poured
out, the mass of mountains described ander the head of Porphyritic
Trachytes have been thrown up. which fact accounts for the abrupt
bending of the trachyte northeast of station 70, and the general slope
toward the Gunnison. The subsequent erosion has been sufficient to
remove the trachyte around station 31, and on the ridges running
southward from this mass of mountains. The amount of the denuda-
tion on the Gunnison is measured by the distance between the top of
tilie mesas and the level of the River.
BASALTIO AEEA&
The basaltic rocks of the district all closely resemble each other.
They are generally dark-colored, gray to black, and are fine-textured.
Tbey contain olivine, sometimes free quartz, the latter not abundautlyi
and on being pulverized magnetic iron can be extracted from them.
The latter always caused a great deflection in the needle at all stations
made on these areas. Vesicular varieties occur in many places. The
different varieties, however^ will be described as we proceed. The short-
ness of the time at our disposal in the preparation of this report pre-
cludes the possibility of giving definite analyses of the rocks.
As already stated, the basaltic rocks are confined to the northern
part of the district, where they generally form the capping of plateautji
or mesas, showing that they are lava-flows. Their source was probably
to the northward, as, with the exception of one locality, I could find no
evidence of their having originated within the limits of our region.
As the general features ot the country have been already given io
considerable detail I will confine myself mainly to the description ot th«
rocks and their mode of occurrence.
Eagle Biver, — On the summit of the ridge southwest of the Eagle
Biver, opposite the second canon, there is an isolated area of volcanic
rock which I call basalt, although I could discover no olivine. Its ap-
pearance, however, closely resembles that of the rocks in the same re-
gion that are un^loubtedly basaltic. It is dark bluish-gray, rather com-
pact, with a slight tendency in places to lamination. There are a few
points of free quartz and numerous yellow spots of some decomposing
mineral, which may be olivine. The area occupied by this rock is lim-
ited, comprehending only about nine square miles. It is shown on map
A. A section across it is shown in Fig. 1, Plate I (/to g). It will be
seen that it rests on the upturned edges of the Bed Beds, and in places
touches the Jurrassic or Cretaceous layers. The section in the figure is
partly ideal, but I think it presents the true relations of the rocks.
It seems that there must have been a fissure through which the mate-
rial was pushed, and afterward spreading out, it covered the edges of the
strata tipped up by the same force that caused the flow. If it is simply
a flow that has spread over the upturned edges of the strata it must
have come from the north. The hills north of Eagle Biver shown at cc,
iu Plate II, are capped with volcanic rock. It is not probable, however,
that this rock is the same flow, although it may be of nearly the same
age. We cannot be exact as to the age, although it is probably com-
paratively modern. All we can say positively is that it is Post Creta-
ceous at this point. I think this flow and the one near the mouth of Eagle
River were contemporaneous. The latter, as I shall show, is of recent
date. It is near the mouth of the river on the north side, and, although
outside of the limits of our district, I wish to refer to it. A more de-
tailed description will be given by Mr. Marvine. The flow had its
source in the hills on the north side. It came down the ravines an4
172« GEOLOGICAL SURVEY OF THE TERRITORIES.
spread out iu tbe valley, covering a space of tbre© or four miles. It
forma a bluff eilge 10 to 20 feet above tbe level of the river. A speci-
men of the rock that I obtaiued is a black vesicular basalt containing
free quartz and olivine. Cn pulverizing it I obtaiued a dark, almost
black, powder from >vhich magnetite could be separated.
This rock is of comparatively recent date, which is evident from tbe
following reasons :
First. Tbe flow has taken place since the carving out of tbe valley.
It occupies the bottom of the valley, which is nearly two thousand feet
in depth, bordering tbe river like the slag |K>ured out from a furnace.
The river seems to be the limit of tbe flow, none of tbe rock being found
on the south side. It was probably pushed by it to the lower side of
the canon-like valley.
Second. The subsequent erosion has been very slight. The basalt is
exposed in a bluff-like wall which reaches to the level of the water,
nothing being exposed beneath it.
Third. The basaltic rock is destitute of vegetation and compartitively
free from any soil. It has the appearance of having just been poured
out. The period during which it was poured out is probably to be meas-
ured by hundreds of years, and perhaps less, rather than by longer
periods.
Grand River, — Below the mouth of Eagle River on the south side of
Grand River there is an area of volcanic rock that has been subjected
to considerable erosion. This area was probably once continuous with
that west of Roaring Pork. Between a creek, Grand River and Roar-
ing Fork it rcBts maitily on beds of Triassic age, forming a plateau-like
surface. Near the mouth of Frying-Pan Creek is a mesa capped with
basalt which is probably a portion of the same flow. This latter, how-
ever, rests on beds of Cretaceous age, as does the volcanic rock west of
the Hog-backs on Roaring Fork. They are all probably remnants of the
same flow. The amount of erosion previous to the spreading out of this
material was very great. The Cretaceous rocks near the Grand, between
Roaring Fork and a creek, seem to have been entirelj' removed. The
subsequent erosion also has been of great extent. The present valleys
and caiions have probably been outlined since, and tbe amount of de-
nudation is to be measured by their depth below the level of the vol-
canic rock.
The capping of the hills west of Roaring Fork is very irregular.
There remain only the remnants of what was once a connected mass.
Station 16 was located on the western edge of one of the patches of
basalt.
In almost all of the valleys drained by tbe southern branches of the
Grand, between Roaring Fork and the plateau of station No. 48, there
are great numbers of volcanic bowlders, derived ftom tbe bills that are
capped irregularly with basalt. The hills themselves are so covereil
with dibris that it is diflicult to define the boundaries of the basalt
The plateau on. which station 48 is located is also capped irregularly
with basalt. Since the flow it has been subjected to a great deal of
erosion, and now tbe basalt is found only in isolated msusses, like that
on which we made station 48. The latter is a mamraallary process
rising 248 feet above the general level, and about 200 feet in diameter.
The following is the section of this curious born-like point, which can
be seen from a great distance in every direction :
1. Dark-gray basalt, containing a large quantity of olivine, also free
quartz s[)aringly. It is a very hard and compact rock.
2. Purplish basalt. This layer is slightly vesicular. It contains the
same minerals that are seen in No. 1.
PIAL8.J GEOLOGY — BASALTS — iFLATEAU CREEK- 173
3. Yesicalar basalt. Mostly red in color on weathered surfaces.
Some of the pieces found at the base are black, and have cavities lined
with carbonate of lime.
4. Tafaceons layer, of which oi^ly the upper portion could be seen.
The color is white, and in some places the layer has masses of basalt.
In layer No. L I found the following minerals, besides those mentioned
above: Hyalite and quartz in segregations and pyrites coating the
weathered surface in a few instances. All these basaltic rocks have
magnetite. The local attraction on the station was considerable.
Tbe cone on which station 48 was located is situated iu an isolated
patch of basalt of the same character (see map 3). There are several
other areas from which pointed and cofflu-like masses rise, none, how-
ever, reaching the altitude of station 48. The basalt, as has been men-
tioned in a previous chapter, rests on dark-gray shales which weather
to a chalky whiteness. This is beautifully shown on the north side of
tbe Grand. It was impossible to tell from the station how extensive
tbe area covered by the basalt is to the north. On this plateau the
area does not exceed eighteen or twenty miles. To the westward it
leaches its limits at least five miles east of station 50. West of the
basaltic line the plateau becomes broken: the capping having been re-
moved, the soft beds beneath yielded readily to. the eroding influences,
and, therefore, instead of a plateau there is a sharp ridge, gradually de-
creasing in elevation to the westward. The course of the range, for it
forms a very well-defined range, is generally west. It is very irregular^
however, and the streams on either side cut profoundly into the strata.
Station 48 has an devation of 11,063 feet above sea-level. Two and
a half miles west the top of the basalt is 150 lower, and two miles farther,
that is, four and a half miles west of station 48, it is 350 feet below it
So we see there is a slope to the westward at present. We cannot tell
whether this is the original surface, or whether it has been modified by
subsequent erosion. It is probable, however, that the original slope
was to the westward. We see the same decrease in elevation from east
to west on the plateau between the Korth Fork of the Gunnison and
Plateau Greek. On station 43» which is one of the most eastern of the
basaltic points on this plateau, the elevation is 11,134 feet. At station
44, one mile farther west, it is 11,128, while on station 45, eight and a
half miles west of station 43, it is only 10,954, a decrease of 180 feet.
Five miles west of station 45 the elevation is 10,904, which is practically
the same as that of station 45. Sixteen miles west of this point, at the
north end of the mesa, the elevation is only 9,800 feet, and at the south
en6, which is three and a half miles farther east and sixteen miles south
of the north end, it is 9,733 feet. This is a fall of a little over 1,400 feet
from station 43, in a distance of about twenty-seven miles. The greater
part of the decrease in elevation is in the western portion ; that is, in
tbe last twelve miles. As is evident, on glancing at the figures given
above, the eastern portion varies but little on comparing the higher
points with each other. AlK>ut stations 43, 44, and ^ the basalt forms
points that rise considerably above the general level, while the sur-
rounding country is very much broken up. To the westward, however,
the basalt forms a mesa-like capping to the country. This mesa is
fiomewhat irregular in outline, forming at first a narrow strip which
divides into two arms, one extending to the southwest and the other to
the northwest They are separated by a small creek that drains into
the Gunnison. It has cut gradually deeper and deeper until the basaltic
eappiug has been removed, leaving a tongue-like process of Tertiary
rocks ^tween the arms.
In the eastern part of the divide the arena covered with basalt are
174
GEOLOGICAL SURVEY OF THE TERRITORIES.
irregular. The highest points iu these areas hardly mark the origins
Burface of the flow. The sabseqaent deDadation has been enormoua,
will be readily conceived when we compare the elevations of th(
points with those of the deepest vaUeys near them. Stations 45 ai
48 are almost on ^ line with each other running north and souti
This line also passes through our camp No. 45 which was on Plat<
Creek. Comparing the elevations of these three points we find that tl
creek at camp 45 is 3,801 feet below station 48, and 3,870 feet helot
station 45. Farther down, the distance from the north end of the mi
to the level of the creek is over 4,000 feet The south end of the m<
is 4,077 feet above the level of the Gunnison at a point due south of
These figures will give some idea of the immense amount of matei
that lias been removed since the flow of lava took place, and show al
how improbable it is that the original surface still remains.
The two plateaus that we have just desc^ribed are evidently the remaii
of what was once one continuous mass. The elevation of station 48
practically the same as that of station 45. On comparing the
from the two localities, we And that they are identical in appearai
and in structure. We have also seen that there is the same slope
the west on both. If they had not been connected we would And tra<
of the flow in some of the valleys, but we search in vain for any su^
evidence. No basalt is seen in the valleys save the bowlders that h:
been carried down from the plateaus. What the original limits wei
is impossible to tell.
It is difficult to get at the exact thickness of the basaltic flow
originally spread out. At present it is probably considerably 1<
At station 48 the total thickness is 248 feet. This is the highest poi
on that plateau but it hardly represents the original thickness,
thickness at the north end of the mesa is 100 feet. The latter may
be absolutely correct. It wns determined from station 57 by angles
the top and base of the abrupt wall of the mesa. The actual \u
may be covered with the talus so that it is concealed. As to the
and the source of the basalt we cannot say anything very definite,
is, however, in all probability comparatively recent, although older tb^
the fiow mentioned as occurring near the mouth of Eagle River,
rests on sandstones and shales of Tertiary age, which were but lit
affected by erosion previous to its pouring out. I was unable to fix
any point as its source; I think, however, that it lies farther to
north. The surface* of the plateaus is covered with good grass, ai
groves of cottouwoods and pines, among which there are uumei
beautiful little lakes. Both of them are very well watered. Ni
station 45 are three beautiful lakes, two of which head streams fl<
ing to Plateau Creek, and one heading a branch of the North Forkj
the Gunnison. Near station 45 there is a beautiful illustration of
effiects of cooling, in the hexagonal columns into which the mass
separated. They are very regular, and are Ave or six feet in diamet
The surface of the mass inclines to the northward.
The edge of the mesa portion of the plateau is very abrupt, esx)ecii
on the western side, and at the extreme northern and southern em
It stands out like the wall of a fortress. The outline is irregular,
accompanying map will give a good idea of it as also the areas cov<
by the basalt. Fig. 3, Plate IX, shows a section made fh>m the
of the mesa to the Gunnison. On the line A B of map E, a represei
the capping of basalt. In all the valleys of the streams headij
in the mesa there is an abundance of bowlders of basalt. They are
numerous in some places, even on the long sloping spurs running
it, that it is difficult to determine the underlying rock.
J
EGKND
B—M. H^l
CHAPTER IX.
EGONOMIOAL GEOLOGY.
The greater portion of our district, with the exception of the area
along £agle Kiver^ lying within the limits of the Ute reservation, of
coarse no mining operations can lawfully be carried on. Indeed, the
areas in which mineral-deposits are found are limited to the group of
monntains in the southenstern part of the district, and to the gneissic
rocks about the hend of the Eagle. The remainder of the country is
covered with sedimentary rocks, mostly of Cretaireons and Tertiary age,
in which mineral deposits are rare. Lignite is found, but, with the ex-
ception of that near station 34, it is of poor quality.
GOLD.
On Eagle River we met a party of prospectors who claimed to have
foaud gold in placer diggings in paying quantities on some of the
streams flowing into the Eagle from the south, below the mouth of the
Pioey, and above the second canon.
On the North Fork of the Gunnison, southwest of station 2G, we met
auother party, who said they tried the dirt, and that the colors were
good.
SILTEB AND LEAD.
The Elk Mountiun mining district was described in the report for
1873. The ores are mainly silver- bearing galena. There are doubtless
oatnerons lodes similar to them at various points around the heads of
Slate River and Rock Creek. We did not have time to make u detailed
Barvey here. The rocks are penetrated in all directions b^' dikes. At
the head of '^ Oh be Joyful " Creek, east of station 32, Mr. Holmes got
a specimen of galena associated with pyrites.* Ou the other branches
ledges would probably be found on searching for them, as the rocks are
similar.
COAL.
Lignite is found at several points in our district. At the mouth of the
Gunnison, and in the bluffs on the ri^*er from the mouth to the mouth of
Koobideau's Creek, it is seen, but of poor quality. This lignite is of
Cretaceous age, being found in the sandstones of the Dakota group.
On Coal Creek, a branch of Anthracite Creek, a bituminous lignite is
foaud in sandstones, which I have referred to the Upper Cretaceous.
Two specimens from this creek were examined, with the following
resalts :
Analyris.
Sped men Spedmen
Ka 1. No. S.
Water 5.04 ) ^^^
VoUtilo matters 31.40 J "^"^
I Carbon 69.fi0 69.68
Ajih 5.00 4.30
100.00 100.00
This coal is black (brownish-black in powder), has a dull luster, and
Au irregular fracture. The ash is of a light-reddish color. The auulyses
1T5
j
176 QEOLOQICAL SUBVET OF THE TERRITORIES.
show that the coal compares favorably w4th the lignites foand in olbcr
parts of the West.
Anthracite Creek, — ^In the report for 1873 I spoke (page 259) of the oc-
carrence of anthracite coal in the Elk Moantaina. It is found at the
heads of Bock Creek, Slate Biver, Anthracite Greek, and Ohio Creek.
It is probably all of Cretaceous age, and was doubtless originally a
bituminous lignite. The coal at the head of a small branch of Anthra-
cite Creek was found in a bed from 4 to 5 feet thickness in sandstones.
The section has been g^ven in a preceding chapter. These sandstones
were tipped up against a range of trachytic i)eaks, and between the
layers of sandstone, some distance above the coal, is a layer of trachyte.
The strata dip at an angle of 20^ to 25^. This coal is probably a
portion of the same bed from which the coal on Coal Creek was ob-
tained, although in the latter case it is lignitic. The eruption of the
trachyte found near the coal first mentioned probably so heated it as
to deprive it of the bituminous matter. This coal from the head of
Anthracite Creek has a snbmetallic luster, is black even in powder, and
has a couchoidal fracture.
Analysis No. 1.
Water 2.00 } - ^a
Volatile mattere «.50J *-^
Carbon 91.90
Ash (of a dark reddieh-browD) 3.60
100.00
Analysis No. 2.
Water 1.60 } ^ „, j
Volatile matters 3.40$ ^'^
Carbon s 88.20
Asb(sameaBNo.l) 6.80
100.00
These analyses prove the coal to be of excellent qualit3% l^either of
the specimens coked. The percentage of water and volatile matters
and the amount of ash compare favorably with other anthracites.
Oh be Joyful Creek. — The coal on this creek is also an anthracite. It
was discovered in 1874, and the following notes were obtained from Mr.
Holmes, who visited the bed. It is two feet in thickness, between beds
of quartzitic sandstones and metamorphosed shales, which dip slightly
to the west. The coal outcrops about 1,600 feet above the level of slate
Eiver at the month of the creek, two miles up the stream. This coal
probably belongs to the same horizon as the coal on Anthracite Creek
and on Hock Greek. It probably outcrops again at the head of Slate
Kiver. ' A specimeD collected by Mr. Holmes has a snbmetallic luster,
is black, with rusty-colored surfaces from the presence of iron, a fracture
somewhat cuboidal, breaking also into layers. This coal seems to be of
poorer quality than that of Anthracite Greek and Hock Creek.
Analysis.
Water 4.00> |« ««
Volatile matters . — 14. 00 J *^"*
Carbon 74.00
Aah (of a reddish color) *. 8.00
100.06
It would perhaps be more properly described as a semi-anthracite.
The sandstones and shales surrounding it are penetrated by numerous •
dikes and mineral lodes.
rSAULl
GEOLOGY — ANTHRACITE COAL.
177
Bock Creek. — ^The coal on this creek is also an anthracite. It is foand
in Gretaceons shales beneath a mass of trachyte. The shales represent
a horizon at lca«t 3,000 feet above the Dakota gronp. The bed is 5 feet
thick.
The following is an analysis of the coal. It has .a brilliant Inster,,
ooDchoidal fractnre.
Andly9is.
Water and Yolatile matters 7.4
Carbon 88.92
Ash, (reddish).
3.68
100.00
The following is an analysis of coal from this region (probably from
Sock Creek) by Professor Mallet, of Colorado:
Fixed carbon i 91.08
Ash of dark-brownish color 5.30
Volatile matters, chiefly water 3.68
100.00
The analyses given above show a decided advantage over the lignites
found in other parts of the Territory, and their occurrence in the midst
of 80 many deposits of galena, nearly all of which is probably silver-
bearing, will probably in the fatnre have a decided and important bear-
log apon the mining operations that may be carried on in this region.
The following table gives the comparison of average percentages of con-
stitnents of the Elk Mountain coals with those of anthracites and other
varieties, of both foreign and domestic. It will be seen that the coals
of which analyses have been given above rank high in the comparison.
Average of wa-
ter and vola-
tile mattera.
Carbon.
Ash.
Variety.
1
s
1
87.96
1
8
90.49
1
m
9.31
9.85
ia30
1
1.58
8.90
8.70
Sl935
5.348
7.661
Bemarks.
Fmign anthracites. .
a537+
98.56
4 analyaea, taken fW>m Dana's
Minendogy: looalitiea, Sooth
Walea an? Hanorer.
PMuaylTanla anthra-
citet.
5.811
94.10
90.83
ea5i
74.55
8a 046
7 analyaea, from table in Bogera'a
Goologtcal Surrey of Pennsyl-
▼ania, rolamo 11, part U.
PWDtylTania aemi'
anthmcitea.
10.106
88.070
10 analyaea, from table in Bog-
ers'a Gkmlogioal Survey of
Pennaylvania, vol ii. iMUrt U.
AMhnMllesfyoMtbs
Ilk MoailalBR,
Csisraio Territory.
7.7S6
M.M
74.00
M.804
8.00
B.68
5.476
Boialt of 5 aaalyMs flveo
above la the ehapcer preestf-
Sag this Cable.
PMBsyWania bita-
laiaooa ooala.
8&888
70.68
69.37
56.80
71.756
1L75
aoo
13.00
ia5o
9l07
1.41
1.80
8.09
5.763
10 analyaea, tnm table in Bo|c-
era'a Geological Sorvey of
Pennaylvania, vol. ii, part 11.
Foteicn Utamiaoaa. .
TSlSO
81.196
1604
10 analyaea, taken from tfana'a
Mineralogy.
»
Ohio ooala
36.65
64.90
53.50
5a 10
5.18
80 analyaea. ttom Kewberry'a
Geological Beport of Snrvey
of Obio for 1673.
Indiana oeala
48.81
59.00
4150
51.80
ao8
98 analyaea, from OeolofEloal Re-
port of Snrvey of Indiana for
1OT3.
12 H
178
GEOLOGICAL SURVEY OF THE TEBBITORIES.
Avorage of wa-
ter and Tola-
tile matters.
Carbon.
Ash.
Variety.
•
S
ttO
s
i
1
>
i
•a
a
1
1
<
6.948
Sfimarlcs.
*
IlUnoiB cools
41.09
64.90
47.50
52.992
9.eo
9.00
10 analyses, firom Geological Be-
port for 1873, Son-ey of Ilii-
noi&
lii Wtt CUUlfl ..........k
47.81
45.49
6.77
From table of 64 averases of
coal analyses, in Geolbgiad
Report 1870, Survey of Iowa,
White.
MisBoarl coals
41.443
79.98
97.72
40. 816
19.97
9.05
9.096
Ill analyses, fitim Geological
Reports for 1873-'74, Sorv^
of Missouri.
Poreign lignites or
brown coals.
3L596
71.71
47.46
60.414
14.95
0.59
7.591
10 analyses, f^om Dana's Min*
eralogy.
Lignites of Colorado
and l^ew Jdexico.
41.984
59.72
44.44
59.364
90.90
2.00
5.616
14 analyses, from table of proxi-
mate analyses of lignites. Re-
port of A. R. Marvine, United
States Geological Survey, Bo-
port of 1873.
Lignites of Wyoming
Territory.
40.979
54.46
47.04
51.316
9.60
1.73
&331
10 analyses, Srom Report of A.
R. MATvine.
Lignites of Utah Ter-
ritory,
59.416
46.84
5d.32
36.35
43.035
7.50
0.97
4.553
6 analyses, from Report of AB.
Marvine.
Liguites of California
53.613
47.83
49.631
4.01
9.96
3.305
10 analyses, from Report of A
R Marvine.
Lignites of Montana
and Oregon.
47.294
04.18
41.9tj
45.44
49.34
12.00
ia55
a 19
7.036
5 analyses, from Report of A. B.
Marvine.
Liguites of Vancou-
ver's Island and
British Colnmbia.
44.4G8
51.81
47.552
9.15
6.94
■
The excellent tables and notes on the western lignites in Mr. Mar-
vine's report for 1873, and the notes on the lignites east of the mount-
ains in the reports of Dr. Hayden and Mr. Holmes, preclude the neces-
sity of any farther remarks here.
GYPSTJM.
Gypsum is the only remaining mineral of economical Importance in
the district. The localities and general description have been given in
previous chapters. It occurs in quantity on Eagle Biver and Fijing-
Pan Creek.
The list of minerals given in the catalogue accompanying the report
is, of necessity, small, the sedimentary formations prevailing in the dis-
trict, being sandstones mainly of Cretaceous and Tertiary age.
CATALOGUE OF MINERALS NOTED IN THE AREA ASSIGNED
TO THE SECOND OR MIDDLE DIVISION, UNITED STATES
GEOLOGICAL SURVEY, IN 1874.
Agate. Cloudy, of white, brown, and gray colors, on the plateaus Ih^-
tween the Grand and Gunnison Rivers. Moss Agate^ of poor variety)
in the valley of the Gunnison River, west of the mesa, near the Grand.
Amphibolk. Hornblevide in small needle-like crystals, in some of the
FIALB.]
GEOLOGY— CATALOGUE OF MINERALS.
179
rocks in the volcanic breccia, near station 31, at the head of west fork
of Ohio Greek.
Caloite. In the Gretaceoas rocks on Grand Biver and on the Gnnnison
Biver.
Coal. Bituminous lignite on south fork of Anthracite Greek. Anthracite f
on Anthracite Greek. A poor quality of lignite is found also in the
bluffs at the mouth of the Gunnison.
Feldspar. Undetermined varieties in the schists at the head of Eagle
Biver and in the Grand Ganon of the Gunnison. Sanidine in the
rhyolites and obsidian on the Gunnison Biver. Trachytes of Elk
Mountains. .
Gold. Said to occur along the upper part of the north fork of the Gun-
nison and head of Eagle Biver.
Gtpsum. In the gypsiferous sandstones on Eagle Biver and on Grand
Biver and Bearing Fork. In the Gretaceous strata of Grand Biver
and the Gunnison.
Chalcedony. Blue variety, lining cavities in the rhyolites on Gnnnison
Biver, above the Grand Canon. White^ in valley of Gunnison, west
of mesa, above the Grand.
Htalite. In the basalt on station 48, near station 73, on Gunnison Biver.
HoBNBLEKDE. {See Amphibole.)
Jaspeb. Bed in color, in chips on the plateaus, between the Grand and
Gunnison Bivers. In nodular limestone in the bluffs on Gunnison
Biver near station No. 60, also near station 73.
LmoNiTE. Near the head of the south fork of Anthracite Greek.
Mica. Undetermined variety, probably Musoovitej in schists of Eagle
Biver and Gunnison Biver. Brown variety in rhyolites in Gunnison
Biver.
Obsidian. Beneath the trachyte on Gunnison Biver, above the Grand
Gaiion. It is both porphyritic and spherulitic.
Ptbite. Octahedral crystals near station 32, Anthracite Greek. Coat-
ing surfaces of basalt, near station No. 48.
Quartz. In the schists of Eagle Biver and theXrunnison; crystals in the
Gretaceous rocks near station No. 32, at the head of Anthracite Greek.
Sanidine. In the trachytes of station 32, station 30, station 34, &c.; also,
in the obsidian and rhyolite on Gunnison Biver, above the Grand
Canon.
Selei^ite. In the gypsum beds of Eagle and Grand Bivers. In the Greta-
ceous shales at various points along the Gunnison Biver.
Tremolitb. In radiating crystals in the porphyritic trachyte on station
No. 38.
Lignite. {See Coal)
CATALOGUE OT BOCKS COLLECTED IN 1873 BY A. 0. PEALE, MIDDLE DIVISION
UNITED STATES GEOLOGICAL SUBVET.
Na
1
S
3
i
5
6
7
8
»
!<►
11
12
I7ame, &o.
Locality.
Porphyry
do
do
Gray ailicoona sandstone (Cretaceoos)
Mottled limestone (Cretaoeonst)
Selenite.
Gypsam
Greenish sandstone (Cretaoeonst)
Gray sandstone, Cretaceous
Gteenish sandstone
Mines on Mount Lincoln.
Da
Do.
Station No. 0, on Eagle Biver.
Below station No. 7, on Eagle Blrer.
Sooth of Eagle Biver, near station No. 6.
Near the Junction of Eagle and Grand Bivers.
Da
North side of Eagle Biver, near its month.
Station No. S0, west of Bock Creek.
Anthracite Creek, near Mount MarcelUna.
Da
180
OEOLOOICAL SURVET OF THE TERBITOBIES.
Catalogue of rodcs ooUtoted in 1873 hy A, C, PeaU, ^*c. — Continued.
Ko.
Name, &c.
13
14
15
16
17
18
19
90
31
»
94
95
96
97
98
99
30
31
39
33
34
35
36
37
38
39
40
41
43
43
44
45
46
47
48
49
50
51
59
53
54
55
56
57
58
50
60
61
69
63
64
65
67
68
70
71
Porpbyritio trachyte, fh>in dike in sandstoDes
do
PorphyriUo trachyte
do
Brown trachyte t from hreoda .,
......do
Dark greenish trachyte t from breccia
LiK^t reddish tn& from breccia
Black traohytef from breccia
Greenish trachyte f from breccia
Black trachyte f from breccia
Dark gray trachyte from breccia
Light gray homblendio trachyte ftt>m breccia.
Oreenfoh laminated trachyte from breccia
Ashy-gray tafa from breccia
Trachyte T (dike No. 1 in Cretaceoos rocks) ...
Sandstone conglomerate
Trachyte (dike No. 9 in Cretaceoos rooks)
Trachyte (dike No. 3 in Cretaceoos rocks)
Trachyte (dike No. 4 in Cretaceoos rocks)
Porphyritio trachyte (dike in Cretaoeons sand-
stones above coal-bed).
Porphyritio trachyte 1
Trachyte
do
Trachyte (dike in Cretaceoos rocks)
Sandstone (above dike)
Poi-phyritic trachyte
do
do
Trachyte (dike)
Sandstone (above dike)
Bed basalt t
Black basalt f
do
Black basalt
ArgillaceoQS shale
Black basalt
ParpUsh basalt
Black basalt
Amygdaloidal basalt
Red vesioolar basalt
Tafa
Black basalt
do
ArgiUaceons shale (oaloareoas Cretaceoos)
Whitish trachyte
PorpUsh trachyte
Porphyritio obsidian, with spheroles
White tnfk
Gray trachyte
Porphjrritic obsidian
Porple vesioolar rfayolite, with hyolite and
chalcedony in the cavities.
Light trachvte
Parple trachyte
Purple rhyoUte
Tafaoeoos trachyte (in breccia)
Trachyte in breccia
Trachyte, greenish, in brecoia
Locality.
Anthracite Creek, near Mount Maroellina.
Da
Mount Maroellina.
Da
West Fork of Ohio Creek.
Da
Do.
Da
Da
Station No. 31, near the head of West Foik of
Ohio Creek.
Do.
Head of West Fork of Ohio Creek, below ita-
tion 31.
Do.
Do.
Do.
Ridge southeast of Station No. 39, between head
of branches of Slate River and Ohio and Aa>
thraoite Creeks.
Do.
Da
Do.
Do.
Small soothen branch of Anthracite Creek, near
the head of the creek.
Station 30, head of Ohio Creek.
Station 3J» between the North Fork of the Gon-
nison and Rook Creek.
Ridge below station No. 34, west of Coal Creek.
CoalCreek, near camp 36.
Do.
Summit of station 38, east of Smith's Fork of the
Gunnison.
Slope of station 38.
Station 39, east of station 38.
North side of Smith'sFork, near foot of station 3&
Do.
Station 40, north of the North Fork of the Gob-
nison.
Da
Station 49, between North Fork of Gunnison and
branches of Grand River.
Station 45. northwest of station 49.
Ridge leading to station 47.
Summit of station 48, south of Gvaad River.
Slope of station 48, south ot Grand River.
Base of station 48, south of Grand Rtver.
Do.
Do.
Do.
Do.
Tot> of mesa, near station 54, south of Grand
River, norUi end.
Top of mesa, near station 59, south end, east of
Gnnniaon River.
Bluff on Gunnison River, below station 60.
Station 71, on Gunnison River.
West of station 71, on north side of Gnnnisos
River.
Da
Above station 73, on north side of Gnnniios
River.
Do.
Do.
Do.
Do.
Station 77, on north side of the Gunnison, near
the Grand CaSon.
Do.
SUtion 79. on south fork of Smith's Fork of Um
Gunnison.
Do.
Do.
REPORT
OF
F. M. ENDLICH, S. N. D.,
181
Washington, D. C, May 15, 1875.
Sib : I have the honor herewith to submit my report for 1874.
According to instracticus received, I took the field July 14, 1874, as
geologist of the San Juan division, and returned with it to Denver,
Colo., October 19, 1874. During that time more than 3,000 square miles
were surveyed topographically and geologically, including all that sec-
tion of country known as the ' San Juan mining district. The very
rugged character of the region, and the inclemency of the weather,
impeded our progress somewhat, and the latter not unfrequently was a
serious obstacle to the successful and speedy completion of the work.
Four chapters and a '^ conclusion " comprise the accompanying report.
Some difficulty was experienced in finding a suitable basis for classifica-
tion in arranging the material collected. The plan of dividing by
formations was ^opted finally. The first chapter treats of the meta-
morphic area, the second of the volcanic, the third of the sedimentary
area. In the fourth chapter the geology and geognosy of the imme-
diate vicinity of the mining region, as well as the mineralogical features
of the mines, have been considered. A circumstance that will let this
latter chapter perhaps appear somewhat unsatisfactory lay in the fact
that the lodes discovered and claimed had in but very few instances
been worked to any greater extent than waB required by law to hold
a good title. It was impossible, therefore, to study anything, save the
surface characteristics. I beg leave to submit this chapter merely as a
preliminary one, hoping to be able, at some future time, to make inves-
tigations upon the same subject when all conditions may be more favor-
able.
I wish here to express my thanks to Mr. A. D. Wilson, chief topog-
rapher of the San Juan division, and to Mr. F. Bhoda, his assistant,
for their uniform kindness and courtesy during the field-season and in
the office.
To Prof. F. B. Meek I am under obligations for the identification of
fossils.^
Hoping that this report may meet your requirements, I have the
honor to remain your obedient servant,
FREDBEIO M. ENDLIOH.
Dr. F. V. Haydkn,
Oeoloffist in Charge^ JJ. S, Geological and
Geographical Survey of the Territories.
]&3
Library. Jt
Of r\^^rC^\.j^
INTRODUCTION.
The district surveyed, topographically and geologically, by the San
Jaan division, during the field-season of 1874, lies between the 107th
and 108th degrees of longitude west, and between 37^ 15^ and 38^ 15'
north latitude. Besides this, the party endeavored, by traveling down
the Bio Grande to Del Norte, and from there eastward, to connect with
some of the work of 1873, on the southern line of the district then sur-
vey^. Two large rivers, the Bio Grande and the Bio Animas, head in
the region explored, as well as a number of important smaller streams.
Flowing northward, there are, beginning in the east. White Earth Creek,
Lake Fork, and Uncompahgre Greek. Bio San Miguel and Bio Dolores
flow in a westerly direction ; Bio Animas, and its tributaries, Cascade,
Arimosa, Junction, Florida, Vallecito, Finos, and Piedra, flow south.
Kamerons small creeks help to complete a very perfect system of drain-
age thronghoot that section of country, admirable, not only so far as
horizontal distribution is concerned, but also regarding the amount of
water they carry.
As a rule, the character of the country is very mountainous, with
numerous high and rugged peaks studding the mountain groups. It
would not be correct to speak of ranges or mountain-chains in that
country ; the only appellation that can properly be given is that of a
Srotcp of large extent. A marked change in the distribution of the
igher elevations can be observed as soon as the sedimentary forma-
tions are reached, and it is there, that well-defined ridges, of limited
extent, however, occur. Toward the north and west the mountains
fall off steeply into the plateau country, while to the south the above-
mentioned ridges serve as a transitory medium between the high and
the low portions of the district. Kear the southern limits of the re-
gion examined, the. well-known '^hog-backs'' set in, identical in form
with those along the Front range.
Numerous points of great beauty in detail can be noticed throughout
the mountain regions just mentioned. Colors in great variety, exhibit-
ing many shades, are to be pbserved in a number of localities, and
greatly add to the effect produced by the sometimes almost ideal shape
of peaks or ridges. The tendency of volcanic rocks, which compose the
greater portion of our dfstrict, to weather in columns, gives rise to the
tbrmation of thousands of little pinnacles, not unlike Gothic architecture
ill appearance. Bugged and steep is the character of the mountain-sides,
while numerous subsidences produced amphitheaters, with perpendic-
alar walls, sometimes of considerable extent. Owing to the horizontal
stratification of the volcanic flows, and to unquestionable ruptures of
the strata, the influence of atmospheric agencies has sharply carved
the outlines of peaks and small ridges in well-defined forms.
Geologically speaking, the variety offered is not so great. As stated
above, volcanic rocks cover the larger portion of the area surveyed,
while on the west and south sides of it the sedimentary beds set in. A
in^up of metamorphic rocks occupies a prominent position, and is well
marked by its sharp peaks and deep cations.
Altogether, the region is one of very considerable interest to the
186 GEOLOGICAL SURVEY OP THE TERRITORIES.
geographer as well as to the geologist. Although bat little woald be
expected from the volcanic area to occupy the geologist's atteution and
satisfy his desire for new and interesting featores, it was still found to
possess so many nttique characters that it could but be regretted that
not more time dare be given to the study of detail structure and com-
position. Many points of importance must have escaxied notice, because
the rugged character of the country is such that much may be hidden
to the eye of one who cannot command over an almost unlimited amount
of time. It only remains to be hoped that subsequent explorations,
carried out on a larger scale, may find and make known the numerous
interesting localities that are as yet undiscovered. Large as the cou-
tinuous volcanic area is, extending eastward into a portion of the work
completed in 1873, its boundaries have not yet been reached. During
the summer of 1875, the same party will have an opportunity of explor-
ing the adjacent country to the south, and no doubt important facts
will be observed during the survey.
In intimate relation with the geognostic features of the district
surveyed, we fiijd the distribution of the drainage. So marked is the
difference appearing in the plotted sheets, that any one i'amiliar with the
general character of the country, might deduce from the horizontal pro-
jection of drainage the approximate outlines of geological formations.
This would not be possible, were there extant there a large number of
such formations, consisting each of numerous members, but as this is
not the case, the deciding characteristics for each geognostic group are
well defined.
CHAPTER I.
METAMOEPHIO AREA.
The metamorphic area sets in soath of the headwaters of the Bio
Grande, at station 17, and from there continues southward for about
twenty miles, eastward to its extreme limit for twelve miles. For four
miles east of station 17 these rocks follow the course of the river, i. e.,
more properly speaking, the course of the river is determined by them,
and then they bend off southward again, for the same distance, influ-
encing the course of a creek opposite Pole Greek. After that, their
border runs io a southeasterly direction, inclosing all that high mass of
mountains that we have designated as the ^^ Quartzites.'' On the west-
ern side they appro^timatel^ follow the course of the Bio Animas down
to Animas Park, where the sedimentaries set in, occuring likewise also
in the valley. As an estimate, it may be said that this continuous area
of metamorphics covers three hundred and fifty square miles. A num-
ber of smaller patches of the same class of rocks occur at various other
points, but are of less importance. The lowest portions of Cunningham
Gulch contain a continuation of the area from station 17 ; northwest
of the Bio Grande Pyramid (station 21), a coarse-grained granite crops
out near a little lake. The cafion leading down northward from Han-
die's peak (station 14), contains a similar granite; on Lake Fork
Greek, opposite station 12, granite again occurs, forming a few small
hills, and it is found also around station 7, extending for some miles
along the base of the ridge. In the lowest part of White Earth Gallon
a schistose rock crops out, that must be referred to this group. It is
overlaid by trachytes, and covers but a small area.
This large metamoiphic group, from a geognostic and geological point
of vieW| is one of the most interesting features that the district presented.
Lithologically considered, almost every variety belonging to that class
can be observed, although the mineralogical variations are not great.
Kear the northern border and toward the middle, quartzites and schists
predominate, while granite appears toward the east and south. Mostly
the quartzites are of a white or gray color, gradually becoming filled
with mica or chlorite, thus turning into schists. Numerous small veins
of white quartz traverse this rock, which must at one, or perhaps vari-
ous times, have been subjected to considerable strains, whereby the
small Assures were produced. At station 17 the rock assumes very
much the character of a gneiss ; the mica is black, quartz gray, feldspar
whitish, but only little of it, texture and structure gneissoid. Going
but a few miles to the north, this description will hold good no longer.
Although for some distance volcanic rocks cover the schists, there is no
doubt in my mind that the two — that of station 17 and that of Gunning-
ham Gulch — are in connection with each other. The feldspar, howeves,
and the mica have disappeared and are replaced by chlorite. Structur-
ally there is no marked difference between them j it is expressed miuer-
alogically only. Again, traveling southward from station 17, we first
find a large quantity of a gray micaceous schist, rich in quartz, and soon,
near station 25, the mica begins to disappear, so that we have a gray
quartzite. This is the predominating rock throughout the highest por-
187
188 GEOLOGICAL SUBVET OF THE TERRTTOBIES.
tions of the ragged group, that'has tberefirom received its name. Local
variations occar qnite freqaently, bat cannot be considered as the rale.
Extremely varied and complicated we find the stratigraphical relations
of these quartzites. The only fact thatcoald be observed with any ao-
caracy, and the only one that is of any direct valae, is, that the anticli-
nal axis ranning throagh the sedimentaries farther westward, continaes
east throagh the qaartzites, giving rise to the formation of some of the
highest peaks in the groap. In treating of this axis sabseqaently, this
continnation will also be discassed, and the mention of it here shall saf-
fice for the present. Eastward nearly as far as station 21, the qnartzites
retain their character as sach, not changing into granite nntil near sta-
tion 22. To the soathwest of station 21 the qnartzites dip regalarly in
a northerly direction, at an angle of aboat 16^, and are overlaid by
trachyte No. 4, horizontally stratified, showing condnsively that cer-
tainly the later trachytic flows had nothing to do with the metamorpho-
sis, or, at least directly, with the upheaval of the group. At some
other points, which shall be mentioned hereafter, evidence was obtained
that will exclnde the trachytic eruptions entirely from caVising any of
the changes there observed.
Along this edge the quartzite is generally of a light grey or white
color, containing interstrata of grey, fine-grained schists with twins and
single crystals of stauroliteb Mount Oso (station 23), reaching an eleva-
tion of 13,640 feet above sea-level, is within the quartzitic area, but some
distance south of it schists again set m. Mr. Wilson noticed on that peak
a fine- grained, white sandstone, in all probability the one that furnished
the material for the formation of this quartzite. West and southwest
of station 17, the same rock continues, liable to the same lithological
changes as at other points. Station 38 is located on it, from where it ex-
tends southward for about eight miles more, when granite makes its ap-
pearance. The cafions cut into this quartzite are extremely precipitous
and rough to pass through. Well-defined strata of the hard material form
at their edges numerous ledges,which decomposing agents have in vain
endeavored to level. Slides, partly snow-slides, partly rock-slides, have
often polished the faces of the mountains, or sides of canons, so as to pre-
clude all possibility of ready ascent. Glacial action has also had its effect
upon the walls, and is made more evident from the distribution of er-
ratic bowlders. Of this we shall speak below. Owing to the compact
structure of the strata, and the impenetrable character of the material
composing them, but little of the precipitated moisture finds its way to
any considerable depth. In consequence of this peculiarity, the creeks
and streams, if even only flowing a few miles, are very swift and carry a
large amount of water. Wherever the drainage has no rapid fall, so
that the waters cannot flow off, it stagnates, and forms disagreeable
swamps. Owing to the hardness of the rock, and the fact that it so
well resists decomposition and disintegration, the debris slopes appear
to be constantly balanced, and upon being disturbed, the disturber will
not infrequently be greeted by an avalanche of the rocks descending to-
ward him.
A number of large streams head in the Quartzite Mountains, and
receive there a bountiful supply of water. Some of the largest are the
Kio Florida, Bio Piuos, and Eio Yallecito, all of them tributaries of the
Animas, and flowing in a southerly direction. One of the well-known
local features that is produced by the steep character of the Quartzites
is the Animas GaOon, several miles below Baker's Park. This caOon has
very steep sides, and is generally considered impassable. At many
points the transition of quartzite into mica schist or the reverse conld be
observed, but a lack of time did not permit us to follow this out in detail.
WDUCH.] METAMORPHICS. 189
Could it have beeD accomplished, probably some very interesting factls
might have been elicited.
Less in horizontal extent, but jast as well marked in their structure,
are the schists. Scarcely at any point were they found entirely free fh)m
bands of a more decidedly quartzitic character, but are generally easily
distinguishable by their darker colors. They, too, show very much
variation in dip and strike, owing, probably, to small local contortions
and slides. A general dip northwaid on the one side of the anticlinal,
and southward on the other, may be observed, however, and to some
extent determines the outlines of the mountain-sides, their more or less
precipitous character. As a rule they seem to be older than the granite,
but it was not possible to establish this point beyond a doubt, as the
above-mentioned disturbances have produced so many abnormal posi-
tions of the beds with reference to each other that it becomes a matter
of great difficulty to establish their true relations. Schists were found
at no other localities in the district, except in the Quartzite group, and
a few points immediately adjacent. That they extend for some distance
under the trachytes, I am very much inclined to believe, but it must
be at considerable depth.
Kear station 22, the granitic area sets in, continuing from there
southward toward the sedimentary ridges. As a rule, the granite may
be said to be coarse grained, with two feldspars. In contradistinction
to the quartzites the granites form less steep and rugged points, owing
to the facility with which atmospheric agents act upon their mineral
constitnents. Southward this rock sets in, a short distance below
station 23, and from there continues west to the Bio Animas, forming
the bed of that river for about nine miles. All the granite in this
southerly region shows a remarkably regular stratification, not only an
apparent one, produced by the main cleavage-plane of the feldspar or
mica lying in one direction. True to what was stated above, the dip of
the strata is in conformity with that of the quartzites and schists, away
from the anticlinal axis toward the south. Generally it is not very
marked, but still reaches 7^ to 1(K>. All along the Animas we did not
observe the junction of the sedimentaries with the granite. The lattei
was exposed in the valley, while the former appear^ in steep bluffs on
either side. From the dips observed, however, it became evident that
the two were conformable, and later in the season we had occasion to
verify this fact. Owing to the stratification of this metamorphic rock,
and furthermore to its gentle southward dip, it forms rounded bowlders,
in ptmtu^ that bear a striking resemblance to the roches-mout&nnSeSj but
I am not prepared to regard them as such only.
It <nay be well to give the mineralogical characteristics of a few of
the most frequently observed varieties of this granite before proceeding
any further.
a is a coarse-grained variety, composed of orthoclase, oligoclase,
mica, and quartz. The orthoclase is pink, translucent, sometimes in
Garlsbad twins, and is the predominating mineral. No parallel arrange-
ment of the main cleavage-planes can be observed. Oligoclase is white
to Itght-gray, somewhat inclined to decomposition. Mica is black, very
thoroughly mixed in with the other minerals, not crystallized. It is prob-
ably biotite, and assumes when decomposing a splendent brown color.
Quartz is yellowish to gray with a decidedly greenish tinge. It is least
in quantity as a rule. As an accessory mineral, magnetite may be
mentioned. This variety is the one roost frequently found, and ex-
tends, with local changes, certainly from station 22 southward to sta-
tion 52, from there west, past station 48, over to the Animas. It weathers
readily and forms sands and small irregular bowlders, b. Another variety
190 GEOLOGICAL SUBYET OF THE TERBITORIES.
occnrring at many localities, altboagb not coveriDg so extensive an area
as the preceding one, consists of orthoclase, mica, and qaartz. It is fine-
grained, and has, on acconnt of a comparatively large quantity of mica,
a dark color. The orthoclase crystals are colorless, transparent, very
intimately associated with theqoartz and mica» This latter is dark-brown
to black, showing single crystals- Quartz is white to colorless, some-
times grayish. In consequence of the compact texture, this rock
successfully resists decomposing influences, and, wherever found, stands
out more prominently than the one before described, c. A third variety
differs from the two preceding in appearance as well as in quantitative
composition, Orthoclase, quartz, and mica form the crystalline aggre-
gate. The orthoclase is pink, translucent, occurring in very small par-
ticles, and is by far predominating in quantity. Quartz is colorless to
gray, and the mica black, occurring very sparingly. In consequence of
the fact that orthoclase forms the main bulk of the. rock, it has a pink
color, and looks in reality more like a crystalline mineral than like a
compound of separate minerals. With reference to its position to the
two varieties described above, it may be said that it occurs in bands
or strata within the first one. Had it been feasible, it would have been
extremely interesting and important to study the relations that these
distinct varieties bear to each other, and to determine whether their
relative position is constant under the same relative conditions.
A phenomenon of some interest was observed a short distance west-
ward of station 22. Some of the trachytes, belonging to Nos. 2 and 3,
have flown toward the Quartzites, bat it appears that the latter mi^
have been too high for them at the time, and they were not reached.
At the point indicated, a very large mass of the volcanic material has
tallen down perpendicularly for a distance of about 700 feet. This
shows that at one time a cave must have existed there, as the possibil-
ity of the place having been underwashed is excluded by orographical
features as well as by the physical character of the underlying rook.
It has frequently been noticed, that at the junction of non- volcanic and
volcanic rocks, caves were formed, and it seems probable that we have
in this case an analogous occurrence of very considerable extent.
Besides this continuous grauitic area there are the isolated points
mentioned above. Near station 7, the granite is coarse-grained, with
orthoclase only, readily decomposing. Kear Lake Fork, opposite sta-
tion 12, and at Handi^s Peak it is very coarse, with large crystals of
orthoclase and white oligoclase. On the. ridge near station 21 it is of
the same character, with a liairge percentage of black mica, giving it
upon first sight the appearance of syenite. At all these' localities it is
exposed for a short distance only, being covered by the overlying
trachytes. The irregularity in the elevation of these outcrops points
to the fact that either the volcanic disturbances must have had a very
marked effect upon the material the lava penetrated, or that prior to
them already the coo figuration of the country was a much varied one.
I am more inclined to the latter view, from the fact mainly that we
find such a very considerable thickness of the volcanic strata at numer-
ous places, while at others, although the difference in absolute elevation
would not warrant it, this thickness dwindles down to a merely nominal
figure compared with the former.
A question of considerable interest, and at the same time one that I
believe can be satisfactorily answered, is that touching the origin of
this metamorpbic group. Along the northern and eastern borders of
the area covered by the rocks of this series, no evidence was obtained
that would furnish a satisfactory clew to the answer. On the north-
western and southern edges, however, several points were found that
BTOUCH.] METAM0RPHIC8. 191
decide the question beyond a doubt. Station 48 is located on an isolated
patch of Upper Devonian limestone^ surrounded on all sides by granite,
answering in mineralogical description to the first one above given (a).
The Devonian strata are deposited on the granitic strata conformably^
both dipping south 15^ west, with a dip of from 4P to6o. Traveling south-
ward from station 4^ toward station 49, we pass for nearly a mile through
a lower sag, the bottom of which is formed by granite. Eising slightly
on this granite, a steep bluff is soon reached, composed below of hard
qnartzites, with sandstones and limestones higher up. All the strata
dip conformably with the well-defined strata of the granite, in the direc-
tion and at the angle indicated above. From the quartzite into granite
the transition is very perfect, although even small specimens can be
found showing on the one side granite, on the other a granular red
quartzite. Near the top of the bluff the latter is white or yellowish,
becoming red and brown lower down. Finally some mica is observed
in it, and the feldspar appears as such, until the coarse-grained
granite is reached. The metamorphosis is very thorough, and can
be admirably studied at this point. So far as I could decide, the
granite was formed out of a partly argillaceous sandstone, contain-
ing some iron in an oxidized state, while the purer sandstones were
turned into qnartzites. Probably the process of metamorphosis was
a very slow one, and lasted a long time. Throughout the stratifi-
cation is well preserved in all the rocks of that group, but partic-
ularly so in the granite of the locality just described. Even the thick-
nesses of the various strata which have been altered into granite, cor-
respond approximately to those at present exhibited by the superincum-
bent beds. At that point, i. 6., a short distance north of station 48, the
granite overlies the dark schists, which in turn seem to be younger
than the true qnartzites forming the main bulk of the mountains still
farther north. Another locality was observed, where the metamor-
phics showed their mtimate connection with unchanged sedimentary
beds, although not so clearly defined as at station 48. West and southwest
of station 38, on the west side of Animas Canon, there appears in the ravine
below the station a coarse-grained, white sandstone, that, from strati-
graphical reasons, I refer to the Upper Silurian. By following out the
course of this sandstone, it will be found that it gradually changes into
a white and gray, very compact quartzite. To establish the precise local-
ity where this change occurs, -did not succeed.
Besides this direct evidence, pointing to the origin of the metamor-
phics under consideration, their geoguostic features are similar, in
fact at many places identical, with those that sedimentaries would have
exhibited under the same circumstances. Not at any point along the
border of this group did we find rocks that were older than Devonian,
with the exception of that white sandstone near station 38. Taking
into consideration, theretbre, the observed conformity of the underlying
metamorphics with the overlying sedimentaries ; taking into considera-
tion, furthermore, the analogous character of stratigraphical relations,
the conclusion must be reached that those sedimentary beds, which
existed below the Devonian, furnished the material for the metamorphic
masses. The presence of the sandstone near station 38, which was not
observed at any other point, speaks for the existence at one time of
sedimentary beds below and conformable with those we now find.
Almost, if not entirely, the Silurian has disappeared, and at some local-
ities only the highest strata of the Upper Devonian remain, while at
others many hundred feet are yet unaltered. Altogether the region is
of the highest interest, and it can only be regretted that very unfavor-
192 GEOLOGICAL SURVET OF THE TERRITORIES.
able weather and a lack of time prevented as fn^m spending as mnch
time there as we shonld have wished to expend npon it.
Another characteristic of that gronp dare not be overlooked, as its
consequences have a more or less direct bc^ng on geognostic features.
Owing to the position that this high mass of peaks takes to the adjoin-
ing low country, rain or snow fall is very firequent. Daring the entire
summer, whenever we had a view of that section of coontry, it could
almost invariably be noticed to rain or snow, and during our trips
through its mountains we had ample opportunity to verify the observa-
tions made from a distance.
It is apparent that, in a case of that kind, glaciers might form that
would have considerable influence upon the shaping of the configuration
in detail; although the falling of dSlnis will frequently produce results
similar to those furnished by moving ice. A number of points were
observed where the rounding off and striation of the sides of canons or
gorges, and the deposition of large, washed bowlders, left no doubt as
to their origin. This was observ^ particularly well on the headwaters
of Yallecito Creek, northwest of Mount Oso (station 23). Near station
38 another locality showing the effects of glacial action was observed.
The hard quartzite strata exposed their edges, having a dip of about 239
to the northwest. From the north and south ridge upon which the
station was located, the ice had come down, rounded off all the sharp
edges of the quartzite strata, and had polished and striated such por-
tions that were too high to be covered. Three or four of these small
glaciers must have moved side by side, separated by narrow ridges.
Toward the main ridge the ground is scooped out dee|>(}r than some
distance from it, and the heads of the upturned strata are worn away
more at the end facing it Numerous small lakes, or, in some places,
swamps, are found in the holows produced by the passage of ice and
rocks.
As mentioned above, some of the granitic rocks in the Animas Val-
ley, above Animas City, have the characteristics of rockes-fnautannSef.
Below Animas City there is a narrow valley aboat one and a half miles
wide on average, and ten miles long, the Animas Park, so-called. The
soil of this valley is composed of drift, originating to great extent in the
granitic areas. Although I should not be prepared to attribute its
presence entirely to glacial action, it seems probable that the ice- masses,
which certainly existed at one time higher up along the river, ihight
have extended, at least periodically^ downward, and thus may have
added their share to the transportation of erratic material. As is al-
ways the case in a comparatively level valley, where the character of
the river-bed offers but little resistance to the eroding influence of flow-
ing water, here, too, the river gradually meanders through it in many
curves, and it cannot be denied that the action of the waters alone
carried perhaps repeatedly over the same ground would be fully able to
produce the result observed.
In a country where the winters are very severe, where the precipita-
tion is considerable, and where the character of the mountains and
canons is sa singularly favorable to allow by far the greater part of the
water to flow ofl', local temporary glaciers may be formed more readily
than where the cited conditions are wanting. Shonld this be continoed
for any length of time, the result will be a series of phenomena analo-
gous if not identical with those observed in regions where persistent
glaciers exist. The absence of any well-developed moraines at the
localities just described, inclines me to the view that such may have
been the case in these instances.
CHAPTER II.
VOLCANIC AREA.
By far the greater area of the district surveyed during the summer
of 1874 is covered by volcanic rocks. ^S^eaily 1,800 square miles of
volcaiiics join on to the region of 1,400 square miles which were reported
npon the year previous (lie[K)rt United States Geological and Geo-
graphical Surv'ey, 1873). It is evident that, where so large a mass of
volcanic material was ejected and spread over the country, that innu-
merable varieties will be found, and considerable difficulty will be
encountered in the attempt to reduce all the observed occurrences to
features already well known.
Orographically this area may properly be divided into three definite
systems — into the —
Plateau country,
£/ii^ country, and
Mountain country.
The first, the Vlaieau country, rises to considerable elevations,
averaging about 12,700 feet above sea-level for the summit. Geognosti-
cally the latter are mostly composed of basalt, although trachyte
plateaus are not wanting. Stations 3, 4, and 5 are located on plateaus
of this character, and may serve as types. Sloping off to the east,
veering around in that direction to the nori/h and south, they present
very steep sides on the west and toward the south. Owing to the high
elevation, their summits are barren, onlj' the rocky debris covering
them. Analogous in appearance, but varying from tbem in every other
respect, is the —
BLUFF COUNTEY.
As such, I mean to designate all those sloping ridges that have been
formed by very extensive flows of the volcanic material, show a plateau-
like summit, but rarely reach the elevation of those before described,
nor the horizontal extent. In contradistinction to them they are inva-
riably formed by trachytic flowd. Deep and precipitous caiions cut
through them, partly the reHult of separation by strain, partly by
erosion. To this class all the lower regions of our district belong.
Frequently they are densely wooiied, or show grassy flats. As a type,
the regions on either side of the Uio Grande, between Lost Trail Creek
and Antelope Park, might serve, varying in elevation from 10,000 to
12,000 feet.
THE MOUNTAIN OOCNTEY
comprises all the western and northwestern portion of the district,
where the highest elevations were found, upward of 14,300 feet, and
which present the most rugged aspect. It is here that the volcanic
rocks reach their highest development, their greatest thickness. Kegu-
larly stratified, the mountains are separated hy narrow but deep canons,
containing swift mountainstreams* This section, too, will comprise all
13 H 193
194 GEOLOGICAL BUBVET OF THE TERRITORIES.
the oreboarinir regioDfl of the San Jnan miniDg district, and from there
over to Mount Sneffels (Rtation 33). While the orograpbical character is
sufficiently precipitous, there is not that regularity which can be observed
in the country of long-continued, raore unitorm flows — in the bluff conn-
try. Although here, too, single strata may be traced without difficulty
for miles, as well as in the former, the mountains or groups containing
them are mostly separated by deep ravines, and the continuity of the
stratum is not so apparent at a glance. The flows that form the high-
est peaks have been of much greater thickness, occurring at a time,
probably, when the bluff country was too high to be reached, but sab-
sequeut disturbances, upheavals, and depressions have endowed the
region with a wild, grand character. No regularity in the arrangement
of the higher portions can be observed, no chains or regular systems of
mountains. Taking the entire high volcanic country into considera-
tion, it cannot be termed otherwise than a group. Upon the strati-
graphical relations of this group — for the flows are so regular in their
succession that we can treat them as strata — more will be s^iid below.
In the drainage, too, of the district, the difference between at least
the bluff and the mountain country can be observed. While, in the
former, the streams run ^ more regular course, one more nearly ap-
proaching the straight line, the creeks and streams of the latter make
numerous turns and curves, probably being forced to do so by the pri-
mary distribution of the mountains, and not the reverse, that the
nountains owe their first form and present condition altogether to ero-
sion. Numerous plaices may be found in this volcanic section where
large masses of rcck have fallen down,'at times, for several thousaud
feet, and are now lying immediately below the perpendicular cliff that
their falling produced.
In speaking of this volcanic area, it will probably be best to divide
it according to its drainage, and after the discussion ui)on that plan is
finished, give the most interesting and instructive points in detail.
A consideration based upon the (^everal strata that are defined below,
might prove satisfactory were it not for the circumstance that so many
streams, mountains, and other localities of the region in question, have
thus far not been supplied with names. Accordingly, therefore, the
main streams and their tiibutaries will be utilized as a means facilita-
ting classification.
The liio Grande, from its head-waters eastward to Del Norte, runs
entirely in volcanic material, as well as all its tributaries from the
norih, while some of its southwestern ones head in the quartzite regions.
W^hite Earth Greek and all its tributaries are within the volcanic area
so far as surveyed during 1874, Lake. Fork and Uncompahgre Greeks
are almost entirely within the limits of this area. Of the Bio Animas
only the head-wateru enter into consideration this time.
Traveling over so large an area of these formations, it soon became
apparent that a certain regularity existed among the various members
comprising the entire system of volcanics. Inasmuch as the flows were
well defined, the breccias easily recognizable, and both could be traced
for, sometimes, considerable distances, the idea presented itself to sepa-
rate the best-characterized groups, and giving them lumbers (analogous
'o the numbering of sedimentary formations), thus facilitate both
lescription and subsequent classification. The absence of well-defined
propylite and andesite, the two oldest eruptive rocks of the Tracbor-
beitic group, is somewhat astonishing, but it seems, from evidence, that
the eruptions of the material in our present district were later than
A of the 1873 district. Besides the large, continuous mass we are
wDuciLj V0LCANIC8. 195
speaking of at present, there are a number of isolated one.s, but nowhere
were the two rocks just mentioned met with. It seems that the magma
which upou cooling produced our present trachyte, was existing in
enormous quantities and gave rise to the numerous varieties that now
reach altogether a thickness of 7,000 to 8,000 feet. Throughout the
entire mass the trachy tic character is constant, changinglooally, however,
ou account of reheating, perhaps. As usual, the tuff's and breccia inci-
dent to the formation of the trachyte are found. Were it not for the
surprising regularity manifested both in a horizontal and vertical direc-
tion, the correct recognition and classification ot the many varieties under
consideration must necessarily be rendered extremely difficult; a) toget her
impossible for the short time that we could spend among them. The
schedule based upon observation of the various strata at numerous-
points will give a general idea of the vertical distribution. Single
features of tho same strata were foc^d to be of great regularity and
materially aided in the identification.
No. 1 is very readily distinguished by the variegated appearance
produced by a succession or change of different colors. Frequently the
white, grayish, or yellowish colors predominate, but pink, red, green,
and almost black are not wanting. In general ai>pearance the members
of this number present the characteristics of a series of "variegated
marl^." They form steep walls, weathering in small columnar masses,
or they show smooth, rounded bluffs, the colors of which are beautifully
blended. Should any isolated hard strata be contained in the series,
they will show themselves as small monument-shaped projections ou
the face of the bluff, or weather in such forms that the play of fancy
can readily picture them as imitations of animate beings. Water-courses
cut deeply into the loosely -cemented material, and aid in forming the
picturesque groups that may otten be observed. On one of the branches
of Lake Fork Creek a very curious group of " monuments " was
observed in the trachyte of this number, illustrated by the accompany-
ing cut. From the high plateau upon which stations 3 and 4 are
located, broken fragments of basalt have rolled down the steep hill and
found a resting-place on a small grassy slope near the creek. Heavy
rain-storms gradually eroded the soft underlying material. This, protected
in the vertical direction by tbe basalt block, assumed a columnar form
in course of time, affording a sufficiently large resting-place to the rock
that has produced this striking result. At the time of our visit, there
were quite a large number of these "monuments" clustered together
in a ravine that had been thus washed out. With theprogress of erosion,
the top of the conical pedestal holding the heavy block must assume
a still more conical shape, and the latter will fall. Several of these
columns were between twenty and thirty feet high. Differing from those
in Eastern Colorado, these monuments do not show smooth sides, but a
corrugated surface, produced by the constant dripping of rain during
storms and other similar reasons.
This trachyte No. 1 reaches an average thickness of about 800 feet
•Wbeu fully developed. It might properly be termed a tuff, although at
layers occur in it that would forbid any such appellation if found
ted. Generally the material composing this series of strata is a
feldspathic aggregate loosely cemented. At some points larger
lents are found among the smaller ones, but all show alike the
rncy to rapid decomposition. The numerous colors that frequently
_ are due to oxygen compounds of iron mainly. At some points,
"M the next stratum above seems to have reached No. 1 in u lit ated
it- lilke upper members are baked and contain jasper and semi-opal.
196 GEOLOGICAL SURVEY OP THE TERRITORIES.
The groap is very clmracteristic and sufficiently constant in its appear-
ance to be recog^nized ; mast not, however, be mistaken for some of the
local accamulations of tuffs that occur in higher trachytic beds.
No. 2 does not show so many variations as the preceding number.
Mainly forming either low plateaus, grassy or wooded, or appearing in
long, narrow ridges, it covers that section of country along the lower
tracts bordering upon the streams of the eastern part of the districts
Frequently caiions are cut through it, and then the walls are mostly
very steep. In color, it shows but little variation. When freshly
broken it has a pink tint, but upon exposure to atmospheric inflaeuoes
becomes brown. Near the border of the volcanic area, it is the forma-
tion most frequently met with. Toward the upper strata (there are
only few in this group), bands and nodules of porphyritic pitchstone,
and of obsidian set in, running parallel to the stratification of the
trachyte. At times they are several feet thick, but rarely extend for
any distance. Between stations 21 and 22, however, one band was found,
from iowT to eight feet thick, that extended for several miles. Twelve
linndred feet may be considered the average thickness for these strata,
the most continuous and easily-traced ones of the entire series. The
rock generally contains a great many small crystals of sanidite; crystals
of black mica are dispersed throughout the entire mass. At some
localities narrow prisms of hornblende occur, dark green to black in
color. Upon exposure the mica assumes a splendent bronze color.
No. 3. — This group can readily be distinguished from No. 2 by the
darker colors shown in its lower member, and the lighter ones its
higher strata exhibit. In some localities plateaus are formed by No.
3, but more frequently it forms the highest bluffs of narrow ridges.
It is divided into two subdivisions, the lower and the upper No. 3.
The former can be recognized by its dark color and its more precipitous
character, while in the upper, the colors are by far lighter and the steep
features less prominent, as it decomposes more readily and therefore
forms slopes rather than vertical bluffs. Lithologically there are dis-
tinctions also, as will be seen below. No. 3, lower, at times shows co-
lumnar structure, and on account of the dark color it assumes upon
weathering, can be mistaken for basalt. Brown is the prevailing color
of the lower members, while the upper ones are lilac, shading into gray
and reddish. For the latter the thickness may be estimated at 1,000
to 1,500 feet, when fully developed; for the former at 800 to 1,000
feet. This formation is well developed at a number of points, and
will be spoken of in more detail when treating of the localities where
it occurs. These two last numbers mainly give the country that ap-
pearance which has induced me to term it a "bluff country,'' a charac-
ter which extends from the I07th meridian to San Luis Valley, of course
with some interruptions caused by local upheavals or other disturbances.
Numerous sanidite crystals occur in the someV^tofies compact, some-
times slightly vesicular, paste; more in No. 3, lower, than in the up|)er
subdivision. Mica is found more sparingly, black when fresh, bronze-
colored after having been exposed to atmospheric influences for some
time. No. 3, upper, contains less sanidite and more mica, and may be
distinguished by the lighter color of its paste. Toward the upper por-
tion of this number a series of beds occurs, that have almost the character
of a paste without any segregated minerals. In color, they are usually
light, compact as a rule, rarely vesicuhir.
No. 4 is by far more varied in its several members than any one of the
preceding series. It is to this group chiefly that the region designated
as "mountain country" belongs, and much of the wild, picturesque
vwuca. J VOLC ANIC8. 197
scenery it contains is due to the brilliant colors some of the strata
belonging to it exhibit. As stated above, the mountains sbow no
iirningement in chains or well-defined systems of ranges, but, in their
detail of form, they certainly deserve admiration and attention. At the
majority of points, where distinct stratification could be observed in the
layers composing No. 4, it was seen to be either horizontal, or very
nearly so. Tbis fact, together with the unequal hardness of the various
strata, produced the result that erosion finally, after other agents i>er-
haps had completed the primary separation, was enabled to carve with
its skillful hand the most unique mountain forms, beautiful in their
symmetry as well as in their detail. Tbe colors of this series are gen-
erally dark, with the exception of those shown by one stratum — the
^'^red stratum.^ Originally white, the color has changed into yellow,
orange, bright red, and brown. A very thorough impregnation of mi-
nute pyrite crystals has produced this change. Upon decomposition of
the pyrite, hydrated sesquioxide of iron is formed, which in turn imparts,
according to the quantities in which it is present, tbe colors above enu-
merated. This stratum is found in the lower half of the series. Above
it the colors are almost invariably dark, a purplish blue, maroon, and
frequently a dark, muddy green. Single bands of lighter rocks occnr in
the upper members. The thickness of No. 4 is between 3,000 and 4,000
feet, containing a by far greater variety of rocks than any one of the
lower groups. Without going into detail, it may be well to give a min-
eralogical diagnosis of specimens from typiral localities.
As a rule oligoclase takes the placeof sanidite,and mica is entirely want-
ing. At some points mica was observed, however, in the lower mem-
bers A triclinic feldspar, that may be andesite, occurs associated with
tbe oligoclase in smaller crystals. In some specimens sanidite was
found, but it may be regarded as tbe exception rather than as the rule.
Tbe paste is microcrystalline to compact.
Above this series of tracbytic beds we find in numerous places such
rocks that must be and are considered as younger. Frequently occurring,
but showicg variations in texture and litbologica} character at almost
every point where it does occur, is the rhyolite. As a rule it may be
found su|>erinoumbent upon tbe beds above described, forming caps for
some of the highest peaks of tbe district. As the rocks underlying, tbe
rhyolite shows a well-defined stratification, conformable to that of the
older strata. At a number of points its character as such cannot other-
wise be determined than by its position and texture, inasmuch as its
mineralogical character would scarcely warrant any positive assertions.
By the aid of partial or full chemical analysis certainly every doubt
can readily be cleared. Near station 10, above 5 miles to the eastward,
tbe most typical occurrence of rhyolite was observed. A deep ravine,
bordered on either side by sloping walls several thousand feet in bei|>hr,
contains in its lower portions a quantity of massive basalt reaching
upward on tbe north wall to more than 900 feet above tbe level of tbe
creek. Kesting immediately upon this we find a series of rbyolitic beds
segregated into narrow strata. It would seem from tbe position of
tbese two rocks', which can correctly be recognized at a glance, that tbe
latter was really younger than tbe former. A!ialogous cases to tbis
have been found in other portions of the western volcanic regions, but
whether they are identical can only be determined by one who has seen
a number of them.
Upon investigation it will be observed that the single narrow strata
of rhyolite lying ufion the bastdt di(> toward tbe valley at an angle of
60O to 70^. There is no evidence that the material could have flown down-
198 GEOLOGICAL SURVEY OF THE TERRITORIES.
ward frotn tbe Dorth nde, prodncing the dip by virtue of any such flow.
Ou tbe coutrary, it bas cume from tbe west. Traveling westward to
tbe bead waters of tbe small creek (we were camped upon a tributary of
Godwin's Creek), it will be neeu tbat with increasing elevation tbe ba-
salt ceases, and a number of small bills are formed by tbe rbyolite. In
any otber direction tban westward, only small isolated patebes of rbyo-
lite are found, fewer of tbem toward tbe east. Considering all tbese cir-
cumstances, tbe conclusion presents itself tbat we bere bave an iustaDce
of intrusive basalt, baviug become intrusive alter tbe flow or flows of
rbyolite bad already assumed a state of rigidity. In no case witbin tbe
district besides tbis one bave 1 found tbese two rocks in the same rela-
tive position. In speaking of tbe country drained by Lake Fork Creek
and its tributaries, I sball bave occasion to enter into tbe detail of tbe
niineralogical character of this and several otber interesting rocks
found at tbat locality.
Dolerite and basalt both occur in tbis district*, tbe latter in by far
greater quantities, however, and in a number of varieties. Tbe three
plateaus upon which tbe stations 3, and 4, 5, and 19 and 20 are located,
are capped by a heavy layer of basalt. Grenerally the color is a dark
gray or black, but in anumberofinstancesit was found to be a brownish-
red, produced by decomposition of the magnetite it contains. These
tbree plateaus strike in one line, approximately north and south, and a
former connection between the two more northerly ones seems highly
probable. Station 3 has an elevation of 12,609 feet, while station 5,
seven miles distant in a straight line, is only 101 feet higher. Both are
located on tbe summit of tbe plateaus, and their elevation shows tbat
there can bave been but very little change in the niveau of tbese beds
independent of each other. It has been mentioned above, tbat tbe
highest members of the trachytic group are to be found in the western
part of the district. This is probably owing to the fact that the eastern
portions were, at the time of eruption, too high to be reached, a view
sustained by the observation just quoted. We find the basalt of these
plateaus* resting upon trachyte ^o. 2, except at stations 19 and 20,
where it covers No. 3. On the summit of the Rio Grande Pyramid
(station 21), we find tbe same case occurring, a cap of basalt, 600 feet iu.
thickness, forming the highest portion of tbe peak. Isolated patches of
basalt occur at a number of points, forming either the caps of peaks, or
presenting, in the lower southerly country, single eruptions of bat
small extent. Station 18, on tbe north side of the Bio Grande, east of
Pole Creek, shows a cap of this kind. Etist of station 10, iu tbe narrow
canon, basalt also crops out, underlying tbe rbyolite. In its specitic
features it is quite interesting at that locality, and shall be spoken of
wore at length hereafter. In color it is there almost black, weathering
brown on the surface. Small particles of olivine are contained in the
niicrocrystalline paste. Prisms of augitl^ occur sparingly. Altogether
tbe rock has a more crystalline appearance than basalt generally diows.
With basalt the list of volcanic rocks found in our district is exhausted,
and we shall proceed to give a synopsis of their horizontol distribatiou
according to the various drainage systems.
A line drawn northward from Del Norte on the Rio Grande, to Sa-
guache, would approximately give the eastern border of the volcanic
rocks. It is there that the blufly chameter is well develop^, ex>utina-
ing westward for some distance up tbe Rio Grande. Mostly of a brown
to reddish-brown color, the perpendicular walls, sometimes several hun-
dred feet in height, give to the country a very characteristic aspect.
Trachyte No. 2 composes these bluffs, allowing an exposore of No. 1 at
■TOUCH. 1 V0LCANIC8. 199
only a few places on the river. The general dip of the flows to which
the bluffs owe their existence is a little south of east, amounting from
2 to 5 degrees, except at points where later local disturbauce^ have in-
creased it.
At Wagonwheel Gap a local phenomenon of some interest occurs.
The flow of trachytic material became somewhat columnar upon cooling,
aod afterward a small hill compofc«ed of it was torn apart, leaving
uearly vertical cliffs ou either side. Through this narrow passage the
river has found its way, leaving on either side of its banks sufficient
space for wagon-roads. Indians have taken advantage of the com-
manding view obtained from the highest portions of the hill, and numer-
cma abandoned ^Uookouts" and low walls along the edges testify to
their preseu<ie in former days^ At that locality, as well as several
others, the trachyte No. 2 contains numerous fragments of jasper,
chalcedony, and flint, sometimes in the form of geodes. Above the gap
the same formations continue without any material change in either
stratigraphical or orographical features. The valley of the Eio Grande
all along there is of considerable width, and the bottom composed of
trachytic drift. To the south and southeast the La Plata Mountains
riae to considerable elevations, consisting probably of trachytic material
alao.
Antelope Park, at an elevation of 9,000 feet, presents some interest-
ing features. To the northeast of the park is Bristol Head (station 54),
the termination of one of the long, high plateaus running southward
from station 2. At its southwest termination this plateau ])re8ents a
vertical wall over 2,500 feet in lieight; then proceeding farther in that
direction, the Santa Maria lake is reached, while on the other side of it
there is an analogous vertical wall, about 1,200 tVet in height. The lake
18 contained in a long narrow valley, partly timbered, partly grassy.
At the east end of thib valley are the Antelope Springs, so called. Upon
examination it will be found that the upper strata of trachytic rocks on
the bluff edge upon which the station was located, correspond to those
on the other side, although they are more than 1,000 feet lower down.
It is a case of sudden subsidence, wheieby the portion on the south-
western side changed both its horizontal and vertical position, while
Bristol Head remained stationary. To the northeast of the station the
strata dip slightly in that direction, while those having fallen, on the
other side, dip at an angle of 6^ to 10^ to the southwest. This dip
shows that the subsidence was by no means a perpendicular one, but
tbat.the southern side fell more than the opposite. Thanks to the ex-
cellent view obtained from Bristol Head, there could. not very long re-
main any doubt as to the action that produced this result. Beaching
Antelope Park from the west side, an exposure .of the upper members of
No. 1 and the lower ones of the succeeding numbers will be observed.
Physically they are soft, and rapidly yielding to atmospheric and
erosive influences. Opposite that exposure, which is soon hidden from
Bight by the secondarily acquired position of the ^Ulropped'^ superincum-
bent beds, the Bio Grande emerges from a narrow c^iiion, and closely
hugging the rocky banks on the bouth side of the park, follows them for
some distance below San Jiuin City. The valley comprising the park
is slightly rising toward Bristol Head, and in it the old course of the
river can easily be traced, it will be found that instead of following
closely along the south banks, which are determined by the trachytic
bluffs of No. 2, the river from its {>oiut of egress formerly flowed across
the entire valley, and, winding along in curving lines, kept a course
much nearer to Bristol Head than the one it has today. It seems
200 GEOLOGICAL SUEVEY OF THE TEBBIT0BIE8.
highly probable, therefore, that at some period previoaa to that at which
the river had the course just described, it flowed still more northerly,
i. €.<f at the time before the subsidence occurred. Counting upon the
regularity shown at numerous other points by the members of volcanic
series, the view muy gain ground, supported besides by other facts, that
the subsidence mentioned is owing to a washing ont of the soft lower
strata. As soon as a sufficient distance whs thus eroded, the rocks
superincumbent changed, by their falling down and southward, the
course of the river. An isolation of the narrow valley lying between
the two vertical walls thus formed, would be advantageous to the for-
mation of either swamps or lakes, and we do in reality find one of the lat-
ter. Its longer axis is parallel to the line of separation of the two ver-
ticHl bluH's.
Still farther ascending the river we find it running in trachyte 'So.2j
which forms steep bluffs on either side, and narrows the canon very con-
siderably at some places. While the elevation of the river-bed is about
9,400 feet along there, the hills on the north side rise to nearly 10,500
feet, reaching trachyte !No. 3. Along some of the ridges this rock
shows very decidedly columnar structure, resembling from a distance
basaltic columns. In color it is dark, and weathers in steep cliflb.
After reaching Lost Trail Creek the higher country begins. Both
south and north of the Kio Grande monntainpeaks become more fre-
quent and their altitudes more considerable than farther east. On the
south side of the river, ascending the main tributaries, we observe the
lower numbers two and three in regular succession and typical develop-
ment. The Rio Grande Pyramid (station 21) is the highest trachytic
point in that direction, 13,773 feet. Beyond that and to the westward,
the volcanic rocks begin to thin out owing to the position of underly-
ing metamorphics. At the time of the flows, the metamorphic regions
must have been sufficiently elevated not to be covered entirely by them.
Although, as shown by small local outcrops, quite an extensive area of
these rocks is covered by volcanics, the high portions, the Quartzite
Mountains, impeded the progress of the eruptive materiaL Along a
line that begins near station ^2, and running northwesterly termiuates
near station 17, the volcanic rocks are overlying the metamorphic rocks,
and while the former show nearly horizontal stratification, the latter
have^ dip of 12^ to 18^ to the northward. Station 24 is a prominent
trachytic point projecting south toward the metamorphic area.
On station 21 a good section of the volcanic rocks was obtained, show-
ing the regular order that has been observed at a number of other local-
ities. The summit is com|>osed of basalt, capping the other rocks, and
having a thickness of 600 feet. Below it there are 200 feet of breccia.
This breccia is composed of numerous large and small fragments of the
underlying strata, and cemented rather loosely by a cement of feld-
spathic character. Then follow 400 feet of a compact gray rock, with-
out any distinctly segregated minerals. It resembles a feldspathic ma-
trix, without any minerals contained in it, and varies in color ftt)m
yellowish to gray, and sometimes pink. Between this and the next
lower member there occurs a band of porphyritio pitchstone, contaiuiug
nuuierous crystals of sauidite, and small decomposing fragments ot
another feldspar. At the point of observation this interstratnm was 8
to 10 feet thick, but as it continues for several miles in an easterly and
southerly direction, variations in thickness occur. Below this pitch-
stone stratum trachyte No. 3 sets in; 400 feet of a light pink to reddish
rock comi»ose the upper portion of that number, followed, lower down,
by 800 feet of the dark-brown laminated trachyte, with much aaniditc
1 VOLCANICS. 201
and bat little mica. A small qaantity of No. 2 is found below this,
weatheriQg very readily into small scaly fragments. This rests upon a
coarse-grained metamorphic granite, which crops out at a number of
points, and is a continuation of that found at station 22. To the west-
ward, about nine miles, the characteristic strata of No. 4: s6t in, forming a
high, flat country, in striking contrast with the adjoining quartzitic
region. This continues upward to the headwaters of the Rio Grande.
Oa the north side of the river, a short distance west of Lost Trail Creek,
there is an excellent development of No. 1, and Nos. 2 and 3 above it.
Very unique blufl's, about 860 feet in height, have the appearance of
variegated marls more than that of volcanic deposit. Presenting a very
marked stratified appearance, it may be observed that this is due mainly
to the accumulation of coloring material (oxygen compounds of iron)
in certain horizontal zones. Not far up the river is this outcrop con-
tinued, however, as it slightly changes its course and the breadth of its
valley. As the dip of the flows or strata at that locality is a south-
easterly one, the disappearance of the lower stratum becomes a neces-
sity, from the position at which they are exposed. Only on Pole Creek,
about three miles from the Rio Grande, and near the junction of the
two, they crop out again, showing, in the former case, fantastic forms
and groups that an enthusiastic admirer might readily construe into
figures resembling human shapes.
Along the north side of the river, the rocks of No. 2 weather in
abrupt bluffs, showing horizontsd seams, and irregular inclosures of
porphyritic pitchstone, that from a distance have the api>earance of
cavities. Above them are the layers of No. 3, dipping conlbrmably
at an angle of 2<^ to 4^, overlaid in turn by the conglomerate that was
mentioned from the Bio Grande Pyramid. About two miles east of
Pole Creek is station 18, with an elevation of 13,656 feet, capped by a
prominent cap of black basalt. This feature will make the peak dis-
tingaishable from any others in the vicinity. Westward of Pole Creek
the character changes; we already begin to reach the section which, in
the beginning of this chapter, was termed the mountain region. Mount
Canby is the first one that presents the characteristic ^' red stratum.^'
We have approached that area which was not flooded by the trachytic
eruptions simultaneously with the regions farther east, and although
only a few miles distant, we find that this peak, at an altitude of about
12,700 feet, shows the lower members of No. 4. Weathering with all
the brilliancy that colors originati'd by ferric oxygen-compounds can
produce, it presents, in its variety of shades as well as its elongated
pyramidal form, one ot the most striking features of the valley. But
a short distance northwest of tliis mountain are the sources of the liio
Grande, which for more than 90 miles flows through one continuous
area of volcanic country.
In concluding the consideration of the formations bordering this river
and its principal drainage, I wish to say a few words regarding the ex-
traordinary regularity shown both in the mineralogical development
and the distribution of the rocks in question. Below the junction of
Pule creek, the most regular development may be said to begin. One
stratum upon the other is found to be in its normal position, and speci-
mens taken miles apart would readily be mistaken Jor those of the
same numbers occurring at other localities. Although deep ravines and
narrow gorges frequently traverse the sides of the long ridges, or even
cut them, this result seems to be owing to anything but very destruct-
ive activity. At some points, certainly along the Bio Grande, the view
can hardly be repelled that the caQous must have been termed by a sep-
202 GEOLOGICAL SURVEY OF THE TERRITORIES.
aration of their two present walls, a separation that was not gradaal,
snch as woald be produced by the erosive action of flowing watera,
but a sudden one. From Lost Trail Cret^k eastward the lower inembera
of the tracbytic system can be readily traced for many milesw The dip
is consUint in the direction the river flows, bat slight. If time could be
spared for a careful investigation of the volcanic rocks along the Rio
Grande much valuable information regarding their horizontal and ver-
tical distribution could be obtained. The extent of the single flows,
characterized as such by their stratigmphical relations and lithological
character, is truly astonishing, aud basing upon this and other evidence,
I have come to the conclusion that the volcanic area surveyed by oar
party in 1873 is but the continuation of the one under mention at pres-
ent.
Flowing in a northerly direction is White Earth Greek, which has re-
ceived its name from the exposure of trachyte No. I. Ascending from
station 6 the caii<m is found to be walled in by vertical or nearly verti-
cal blufi's of No. 2, while metamorphic rocks crop out below. As usual,
they present the rugged appearance common to members of that num-
ber, until the small valley north of station 2 is reached, where the flows
have preserved more of their original form, and show plateaus of no
very considerable extent, however. Above the flrst lower plateau two
more are found, until finally a slope is reached leading up to the station,
an elevation of 13,560 feet. Here the rock corresponds to some of the
members of the higher No. 3. The paste of this rock is compact,
darker than that of the corresponding group generally. Numerous
crystals of yellowish sanidite occur in it, while mica is wanting almost
entirely.
Descending again to the level of the creek, it is found that the strata of
No. 1 crop out tor some distance along its left-hand bank. The rock
here is white to grayish and 3 ellowish, readily decomposed. It is not
so Arm in texture as that on the Bio Grande, and therefore does not
show the picture^que forms that were observed at that point. Higher
up the succeeding numbers set in until No. 3 is reached. At all these
localities the bluff character is well preserved. At many places tbe
rocks are bare of any vegetation or soil, and the traveler rides over the
surface, as it formerly flowed, only with the difl'erence that at present
it shows an easterly dip. Ascending still farther, toward stations 3
and 4, basalt sets in about 400 feet in thickness at the edges of the
continous bluff. A long, high plateau, some distance above tim-
ber-line, stretches from north to south approximately. No soil has
accumulated as yet on the naked fragmenvs of vesicular basalt. Na-
uierous little ponds and swamps indicate that beneath the layer of
fragments, the original flow must be undisturbed. Two varieties of
basalt occur here, the black and a brownish-red. No definite rela-
tion between the two could be recognized, and it seems highly im-
probable that it should exist. Both are vesicular, sometimes hav-
ing the vesicles drawn out to one or two inches in length. Olivine,
a dark green variety, is found sparingly in their niicrocrystalline paste.
Indications of columnar structure may be observed along the precipitous
bluff' on the west and southwest sides, but the columns are not well
developed. Station 5, at an elevation of 12,737 feet, is located a little
west ot south of Ihe two last-named stations, on a similar plateau, which
at one time was probably in connection with it.
These plateaus separate the waters of White Earth from those of
Lake Fork Creek. Near the northern line of our district, between tbe
two last-named creeks, station 7 was located on an isolated patch of
BTOuciLl V0LCANIC8. 203
ba^lt, surroanded on all sides by granite. A short distance south-
ward, however, tbe volcanic area a^i^ain began. Ascending Lake Fork
the two lower members of the trachytic series are met with. Opposite
station 11 (10,611 feet), No. 1 has reached a good development. For
800 feet we tind a series of grayish, pinkish, to red trachytes, weather-
ing iu small fragments. Sanidite and hornblende are abundant in it ;
more particularly the latter. Near the base of station 11 erratic granitic
bowlders were observed ; not iu great quantity, however. It is a coarse-
grained granite, of the first type that is described from the metamorphic
region. Subsequently discovered outcrops of this same granite, a slioi t
distance from station 12, disclosed the origin of the bowlders. About
four miles south of station 11 is San Gristoval Lake, above which the
erratic metamorphic material is found in greater abundance than
farther below. The bowlders are larger, intermixed in the bed of the
creek with numerous small ones and pebbles. Although no distinct
evidences of glacial action were found either on the bottom of the nar-
row valley, or along tbe steep walls inclosing 4t, I am inclined to think
tbat such action must have produced the result observed. The valley
is a comparatively straight one up toihe point where the granite comes
to the surface, and its form is that of a trough. Near the last large
bend, east of station 12, some of the granitic rocks, in pottitUj show a
very smooth surface. Inasmuch as tbe physical character of that
granite admits of weathering that would produce the same efifect, £ am,
therefore, not prepared to assert the existence of a glacier of large
extent at any tormer time, but it becomes a matter of great difficulty
to account for tbe existence of the erratic material at the localities
where it was observed unless that view l)e held.
An interesting leature was observed at the north end of San Gristoval
Lake. From tbe east a rapid mountain-stream flows down into Lake
Fork, near tbe junction of which a large mass of yellow volcanic mate-
rial has been deposited. This matenal was not deposited by any volcanic
activity, however, but was brought down from the eastern mountain-
ridge flirough the channel of the present creek. It seems improbable
that so large a mass should have been carried there by the compara-
tively small quantity of water, so that very likely snow-slides or even
glacial action may have contributed their share. By the means of this
body of soil and undecomposed volcanic material having been lodged
iinmediately in the course of Lake Fork, that creek was dammed back,
and tbe present lake was formed. It seems prbbable that all, or at least
a very large i)ercentage of it, must have been transported to the place
at ouce, otherwise the maiii creek would have been able, gradually, to
cut its way through, and the formation of the lake would thus have
been prevented. Judging from tbe ^^ fresh" character of the surface, it
would seem as if this enormous land-slide had occurred but a compara-
tively short time ago. Small ishinds in the lake, only a few yards long,
with fir-trees growing upon tbem, speak for tbe same view.
As mentioned above, a small amount of metamorphic granite crops
out near the last large turn of Lake Fork, overlaid by trachyte.
Station 12 was located on No. 4, at an elevation of 13,967 feet, the last
prominent point of a ridge running from north to south. This ridge is
remarkable for its beautiful detail form, and for the excellent develop-
ment of the ^^ red stratum." We have again reached the region of high
uiountains, and with it the higher trachytic strata. Ascending still far-
ther up the creek, we soon leave the lower members of the series alto-
gether and are in No. 4. One of the most prominent points near the
headwaters of Lake Fork is Handle's peak, 13,997 feet high. Here the
204 GEOLOGICAL SUBVET OF THE TERRITORIES.
strata of No. 4 are particularly well developed, and afford important in-
tortnatioD as to vertical saccession. As a rule, the paste is of dark color,
a bluish to maroon, sometimes with a greenish tinge, while the feld-
spars contained in it are yellowish. Small crystalline fragments of
feldspar are frequent in the higher strata of this peak, and it is they
that usually impart the greenish color to the rock. The}* receive their
color in turn from a small percentage of protoxide of iron. Near the
summit is a baud of whitish rock, abont 200 feet in thickness, that ap-
pears like a matrix, without any segregated minerals.
Descending from Haudie's Peak we pass over an ontcrop of meta-
niorphic granite, in the short but deep cafion leading down to the main
creek, and there again reach volcanic rocks. Above this point we ascend
rapidly until the pass is reached, leading over to the Animas Forks.
With that the region of ore-bearing rocks begins, and that will be treat-
ed of iu the chapter upon the San Juan mines.
One of the main tributaries of Lake Fork is Godwin's Creek, the junc-
tion of which is opposite station II. This creek drains a very high and
interesting section of country. Single prominent peaks of considerable
altitude are contained in it, and the remainder, partly grassy plateaus,
partly small ridges, is to a great extent above timber-line. Station 8
is located at an elevation of 12,959 feet, on trachyte No. 3, and from
there a good view of Uncompahgre peak, the highest mountain of the
region, was obtained. On the station mentioned, the volcanic strata or
flows dip off to the eastward, inclining slightly to the north. The rock
composing the summit of the occupied point is very hard, has a dark
paste, but weathers brown. Crystals of sanidite occur throughout. Hy-
alite may be found in small cavities or fissures.
Ascending farther up the creek, one of the most important localities
of our district was reached, that about 5 mileseast of station 10, at canip
23. While all other points thus far visited had failed to offer any ex-
planation as to the locality from which the enormous quantities of
volcanic material flowed, the point just mentioned afforded sufficient
evidence regarding that interesting question. Near camp 23, as has
been mentioned above, the only place was found where basalt occurred
in a comparatively low country (10,679 feet), and it was there where
rhyolite was observed to cover it. From the creek upward, on the
north side, steep, dark-colored bluffs rose, cut into many irregularly-
shaped fragments by erosion. Above them a light colored mass of
rocks appeared, showing separation into distinct narrow strata, inclin-
ing at an angle thatreached GO^ to 70^. The former is basalt, the latter
rhyolite. Of compact microcrystallino texture, the basalt showed numer-
ous inclosures of epigene minerals, chalcedony, agate, amethyst,
stilbite, and calcite. The three former occurred in small, perfectly-
filled gcoiles, while the two latter were generally found in fissures and
cracks. Immediately upon this rock lay the rhyolite, in the stated
position. A white to grayish paste, very compact, contains nnmerons
small crystals of transparent quartz wit!i double terminations. Crystals
of sanidite are disi)ersed throughout the entire mass, and small six-
sided ])risms of black mica occur sparingly. Near the junction of the
rhyolite with basalt^ a curious interstratnm was found, only 6" to 8"
in thickness. It is a brown, vitreous pitehstone, containing crystals of
quartz and sanidite but no mica. This stratum was only traced for a
short distance, owing to the precipitous character of the walls, bnt
probably extends for some distance, analogous to the occurrences at
other points. Farther up the valley rhyolitic hills api)ear, light-gray to
white iu color. Ascending the basaltic wall for about 700 feet, the
KDUCH. 1 VOLCANICS. 205
rhyolite is reached, and, recedintj^ toward tihe higher portions of the re-
gion, extends for a vertical distance of 2U0 feet. After this a nearly level
area is traversed, while the ascent for the distance may amount to 100
feet. Above this, however, the trachytic beds are fonnd in their regnlar
gaccession, at first the npper portions of No. 3, then the lower ones of No.
4. It is evident, therefore, that fiom this side no flow of rhyolites could
have occurred, and from any other side the possibility is precluded by
the geognostic features of the surroundings. It is my opinion, therefore,
that the rhyolite occupied at one time a position very near the base of
the valley, and the outflowing basalt caused it to assume that in which it
is found at present. Inasmuch as this was the only locality where we
bad occasion to observe two of the youngest volcanic eruptive rocks
together, my attention was led to the question whether this might not
be regarded as one of the greatest points of outflow, if not as the only
one. Subsequent evidence, derived from the stratification of the flows,
confirmed this opinion, and I have arrived at the conclusion that near
this point the main outflow for the entire continuous volcanic area under
consideration occurred. In speaking of the stratification of the volcanic
rocks this point shall be further elucidated.
Near one of two tributaries of Godwin Greek is Uncompahgre peak
(station 9^, 14,235 feet above sea-level. The summit of this mountain is
formed by No. 3, and the lowest portions by No. 2. At the higher por-
tions of the peak the strata dip from 3^ to 6^ to the northeast, away
from the rhyolitic region that has just been described. The mountain
presents a bold appearance, and serves as a landmark for many miles.
Toward the southwest and west it slopes off more gently than toward
any other, but to the northeast presents a very steep appearance. A
small |>eak, to the south we^^t of Uncompahgre, shows the identical strata,
lower, however, in elevation, and dippiug in immediately the opposite
direction, to the southwest. This fact is of importance, as this peak is
nearer to the center of eruption. A number of high points are found
in the vicinity of Uncompahgre, none, however, reaching the same alti-
tude. Many of them present the same stratigraphical relations.
Flowing in a northerly direction, west of Lake Fork, is Uncompahgre
River, rising near station 28. At that locality the strata of No. 4 have
reached a very good development, and in the ridge containing stations
27 and 28 the red stratum is particularly conspicuous. About four
miles north of station 28, station 29 is located, on the characteristic
bluish trachytes of No. 4, resembling closely those forming the higher
portions of Llaudie's peak. Similar to the occurrence of the white band
near the summit of that peak« we find one here of almost identical com-
position and location. The trachyiic rocks weather in scaly fragments,
sometimes of considerable size but of small thickness. From that point
the higher numbers of trachyte extend northward in narrow ridges, but
little cut by lateral drainage. A tendency to columnar structure pro-
duces along the steep sides of these elongated ridges numerous pin-
nacles, from a distance apparently small. They reach considerable ver-
tical dimensions, however, and may be compared to the ornamental spires
of Gothic architecture. Added to the eflect produced by their form, the
colors they exhibit are an additional factor. Near the head watersof some
of the Uncompahgre's tributaries is ono peak that atti<icted attention by
its singularly regular form, long before it was reached — Mount Sneffels,
reaching an altitude of 14,162 feet. It was our station 33, and
proved to be an interesting point. Horizontally stratified, or with
an imperceptible dip of the strata, this mountain towers far above
its surroundings, rising more than 7,000 feet from the lov^er country
206 GEOLOGICAL SURVEY OF THE TERRITORIES.
to the west. While the higher portions of the peak are composed
of tnichyte No. 4, the last 400 leet proved to be rhyolitic material.
Diffeiiug from the typical rhyolite, its structure and coinpositioD, never-
theless, assign this place to it. On the fresh break the rock ban a
muddy olive-green color, but turns brown upon exposure. Its struct-
ure is somewhat crystalline, owing to the large quantity of feld-
spathic crystals contained in the paste. To the southwest of Mount
Snefi'els a very extensive ^' drop " of the volcanic strata occurred, about
four miles in length, and a little more than a mile in width. Unlike the
one descnbed from Bristol Head, no erosive agent can have occasioned
this one, as there is no connection between the sunken area and any
point from whence such an agent could have operated. The strata have
dropped down perpendicularly for more than 2,000 feet, retaining to
some extent amoug the mass of debris their original connection.
Approaching from the south or southwest, the ridge suddenly falls off
in vertical bluff's, and only the accumulated mass ot broken fragments
enables the descent. We have named this place the ^^ Great Amphi-
theater," as it resembles one in shape. Those strata, that show a partial
connection, are cracked in every direction, traversed by large and
small fissures. Masses of broken rocks are constantly rolling down
the steep sides into the depression, so that in course of tim% much of
the present grand aspect of the peculiar formation will be lost The
ridge extending westward from Mount Sneffels drops off into the Sedi-
mentary bluff' country, remaining volcanic throughout its entire length.
As at numerous other points near the edge of the volcanic area, so the
mountains here, too, show a regular stratification, almost horizontal.
It seems highly probable that subsequent erosion, to a great extent.,
determined their present forms, as it appears incredible that flows of
such considerable vertical dimensions should terminate so abruptly.
Evidence was obtained at several places near this ridge and those
a(\joining that the sedimentary beds held, at the time of the eruptive
flows, the same position they now occupy. They belong to the Cre-
taceous system.
TheSan Miguel River rises in volcanic country, but soon leaves it, and
flows through sedimentary formations. There, as well as near the head-
waters of the Rio Dolores, the trachytes show the same character as
along the ridges upon which station 24 was located. Besides these two
streams the Rio Animas heads in a portion of the high volcanic district^
as well as its northerly tributaries. In the chapter on the mines of the
San Juan region the character of the rocks through which the Upper
Animas flows ^ill be discussed, and for this place, therefore, only some
of its tributaries remain to be described. Bear Greek, heading near
station 30, flows in an easterly direction and joins the Animas in
Baker's PVirk, near Silverton. Ascending that creek from the park
mentioned, the red stratum may be observed following along Mineral
Greek, which branches off to the northward from Bear Greek. The
former rises near station 28, where the red stratutr is very well devel-
oped. Soon, however, after traveling up Bear Greek beyond the junc-
tion with Mineral, sedimentary beds set in, overlaid by the trachyte.
Station 30 is located on the highest point of the ridge separating the
waters of the Animas from those of the San Miguel. Its elevation is
13,897 leet. On either side of the ridge sedimentary beds apt)ear, and
the volcanic rocks only form the capping of the ridgenor isolated peaks.
A considerable amount of metamorphosis of the sedimentary beds has
been proiluced by the action of the overflowing volcanic material. The
Bommit of station 30 is formed by a very i>ecuiiar lock. A microcrys-
4,
V O,
!/*
i .
Fto. S. — LiziRD's Hkai
KBUciL) VOLCANICS. 207
talline paste coDtains ionnmerable small crystals of epidote, replacing
hornblende. At some places the epidote congregates so as to form
narrow veins throngh the rock. Octahedra of magnetite are also found
in the paste, which has a dull gray color. Banidite occurs only on very
minute crystals. Mica was not found at all.
Of interest the ridge running south of Bear Creek from station 30 to
Sultan Mountain will be found. Although no sedimentaries appear in
Baker's Park, immediately across the ridge they set in, covered by tra-
chytes. Their elevation is quite considerable, reaching more than 10,000
feet at those points. Duriugsome former time they were distnrl>ed,
and now the trachytes rest unconforniably upon them. Sultan Mount-
ain, station 26, is the last massive peak of volcanic material on the
downward coarse of the Animas, and reaches an elevation of 13,366
feet. To the south and southwest the trachytic material shows regular
stratification, very nearly horizontal, showing only a slight dip south-
ward. At several points the process of erosion has separated small
patches from the main body of volcanic material. Tbis is the pase at
Engineer Mountain (station 31, 12,971 feet high). A little more than
one thousand feet of light-gray trachyte caps the dark-colored Carbon-
iterons sandstone. The shape of the mountain is that of an elongated
pyramid, with two very steep sides, the one of th^m nearly vertical.
On the latter side the trachyte shows a decidedly columnar struc-
ture, which contrasts sharply with the stratification of the sandstones
below. Lithologically the rock belongs to No. 4. It is a light-gray
crystalline paste, containing crystals of oligoclase dispersed through the
material. Upon weathering, the feldspar decomposes and falls out, giv-
ing it a vesicular appearance^ Small particles of mica are distributed
sparingly. West of Engineer Mountain a sharp ridge extends from
north to south, again showing the capping of trachyte upon sedimentary
beds. With this the consideration of the continuous area of volcanic
material may be regarded as completed, but there are several isolated
eruptions occurring in the district surveyed. One of the largest and
most p^minent is the Mount Wilson group (station 35), of which the
highe8t'\)eak reaches an elevation of 14,280 feet. Immediately north-
east of ihis mountain is the probable point of outflow, spreading from
there tr*the east more particularly. Two of the highest spurs running
from tb ^ main mass are formed by the flows from Mount Wilson, and
rest upon sedimentary strata. Lithologically the trachyte of these
spars w >uld be referred to No. 3. East of the main peak is a curious
luonument of trachyte, an obelisk-like mass of stone placed upon a nat-
ural pe<' stal, of symmetrical form. The formation of this monument,
wbich iJi .s named *^ Lizard's Head,'' is owing chiefly to the tendency to
columnar structure shown by the rocks. Its height amounts to 290 feet,
while at the base its diameter is scarcely over 60 feet. Its summit is
13,160 f \t above sea-level. Toward the outer edges of the group the
t^^^ material is stratified, while on the highest point, Mount Wil-
sOkT . eflnite stratification can be observed. On the summit a rock
occurc ^at may be referred to the Doleritic group. The*rock is dark-
gray to lack, containing a feldspar that very closely resembles labra-
dorite. >mall nodules occur in it that seem to be composed of minute
hombler e crystals, varying somewhat in color.
Anotki. * isolated group is the one upon which station 36 is located.
On the sc -ith side of the Bio Dolores a quantity of volcanic material is
ft und, forming in shape a figure similar to that of the horseshoe. Sta-
tion 36 is one of the high points of that flow or series of flows, having
An elevation of 12,554 feet. From that, and probably two other points
208 GEOLOGICAL BURVEY OF THE TERRITORIES.
more to the westward, the eraptive rocks spread over the highest por-
tions of two parallel spars, couDected by a third ooe. Similar to the
rocks of Deighboring localities we find the lithological character of those
found here. The main portion rests upon Carbouiferoas sandstone,
while the two disconnected ends of the horseshoe have flown over Lower
GretaceoQs rocks. As is usaally the case at the points of ontflow, the
rocks from different altitades vary considerably in their mineralogical
composition. Near the summit of station 36 the rock presents a very
handsome appearance. A greenish crystalline paste contains innnmer-
able white crystals of oligoelase, which are set off to advantage by ac*
companying black crystals of hornblende. Sanidite also occars. Six
hundred feet below the summit the rock is very similar to that descrihed
from station 31 ; a white to light-gray paste, inclosing crystals of oligo-
elase ; mica occurring very sparingly. To the southwest of station
36 is station 37, located npon the above-mentioned red sandstone, but
having on either side, north and south, isolated patches of trachytic
rocks.. Considerable disturbances have taken place at that locality at
onetime, prior certainly to the eruption of the volcanics, but it seems
that their appearance gave rise to new dislocations, and finally a third
era occurred, which was again marked by displacements. South of sta-
tion 37 a series of sandstone strata that had formerly been forced from
their normal position, were still more disturbed by the intrusion of the
volcanic mass. Between these strata of sandstone, layers of about
equal thickness of trachyte are wedged in, forming apparently a por-
tion of the stratified series. (See section.) A secondary dislocation of
about 60 feet vertical distance, has brought the layers of trachyte im-
mediately opposite those of the sandstone, and the reverse.
The La Plata group, at the head of Junction Greek, a tributary of the
Animas, is also one of the isolated volcanic regions. Several small
patches are adjacent to the mountains, covering either Carboniferous
sandstone, or, as was the case at station 42, Lower Cretaceous sandstone.
During the following season, 1875, this region will be explored thor-
oughly, and more light will be thrown npon the specific characters of
the La Plata Mountains.
With this latter locality the volcanic area of the district surveyed
during 1874 is concluded. Small cones, of basalt probably, were visible
from a distance in the Cretaceous country, but were not reached in the
course of our travels. There remains now, yet to be considered, the vol-
canic area as a whole, and the conclusions that may be drawn from the
consideration of the stratigraphical conditions of the rocks.
It will be observed that at all points near the border of the volcanic
area the strata or flows show a surprising regularity in their structure.
Scarcely ever does the dip exceed 2^ or at most 3°, unless some very
local disturbances have given occasion to an increase thereof. As we
approach^ however, from the outside of this area toward the interior
portions, a marked change in the stratigraphical relations can be ob-
served. We find that the high plateaus, the long-continuing bluff's, and
the sfratoid peaks, all show a tendency to dip off from one point, as
from the center of a circle toward its periphery. With this tendency
the dip increases gradually, as we approach that region near which sta-
tion 10 is located. So far as could be observed, the flows show a dip off
from that locality on every side of it, except in the immediate neighbor-
hood, where a number of dips are noticed, falling in toward the depres-
sion east of station 10. This feature is so constant, is, furthermore,
unique throughout the entire district of which this chapter treats, that
I could not do otherwise than attach great importance to it. Taking
ODUCH.1 VOLCANICS. 209
into consideration primarily tbe stratigraphical relations as above given,
the conclusion will present itself that tbis point, or very near ibis point,
mast have been the main region of ontflow; that here is the center from
which tbe greater portion of tbe volcanic material spread over tbe snr-
roQoding country. In support of tbis view are the additional facts
that, at the locality in question, rhyolite and basalt, two of tbe youngest
volcanic rocks of that region, were found in a- caHon in considerable
masses, while at all other points they occupied either tbe summits of
peaks or of extensive plateaus. It seems strange, however, that these
same rocks found here, should occur el8ewbere at such considerable
altitudes. Taking tbe evidence derived from stratigraphical conditions
it would seem tli»t, after tbe flow of volcanic matter bad subsided, a
depression of the place from where it w<)s issued took place.
Another point of great interest and importance is tbat touching the
conditions of tbe country at tbe time of tbe outflow. It was observed
tbroughout, tbat in the eastern portion of tbe district tbe lower num-
bers of the trachyte prevailed, ro the absolute exclusion of tbe highest
ones, while in the western localities this order of things was reversed.
Inasmuch as tbe four adopted subdivisions are found occurring con-
formably,.one upon the other, tbe view that they must have originated
from one point, receives a decided support. Should tbis be tbe case,
then, tbe facts illustrated by the horizontal distribution of the volcanic
material can best be explained by tbe assumption that during the
period of the earlier flows tbe western country was too high to be in-
vaded, while during the later flows the order of things was reversed,
and the eastern portion received none of the younger material. At the
time of tbe succession of flows, tbe region east of station 10 must have
had a by far greater elevation than at present, a fact which is demon-
strated by the occurrence of the youngest volcanic rocks at higher alti-
tudes. It would be extremely difficult to attempt a thorough analysis
of tbe dynamics involved in these grand demonstrations of volcanic
activity, and particularly so after a survey that has been so limited in
time as ours. *
14 H
CHAPTER III.
SEDIMENTARY AREA.
After leaving the area covered by volcanic rocks, and traveling in a
aoutherly direction, the diftbrence of geological formations can at once
be recognized from the configuration of the country. Instead of high,
rugged mountains, arranged in groups, without any reference to chain
or range systems, we here find a series of approximately parallel ridges,
tapering oft* gradually to the southern plains. While a great portion of
the volcanic district reaches above timber-line, the mountains or hills of
the sedimentary region are timbered, and the valleys between the ridges
show fertile, grassy soil. Although the variation in the litbological tbrma-
tions is not very considerable, it can, nevertheless, be readily fecognized
from the orographic features of the country. Bordering immediately
upon the southern and western edges of the metamorphic area the sed-
imentary beds begin, extending from there south and westward, with
only small interruptions in the latter direction, caused by local volcanic
eruptions.
As stated in the chapter on metamorphics, the lowest members of the
geological series have almost entirely disappeared, leaving only small
remnants that cannot even be positively referred to any definite group.
A portion of the Devonian rocks have escaped the influence that meta-
morphosed underlying beds, and offer an interesting field for study,
partly on account of their contact with the metamorphosed material,
partly on account of local features they exlHbit. Above them the Car-
boniferous formation set« in, greatly varied in its several members, and
retaining characteristic variations over a comparatively large area.
After this has been passed, a gap occurs in the adopted succession of
geological formations. The Triassic and Jurassic beds are wanting in our
district. Immediately above the Carboniferous the Cretaceous strata are
found, as it would seem from some exposures, resting nnconformably
upon the former. These continue for a considerable distance down into
the plains, so far as our survey was extended, without being succeeded
by Tertiary deposits.
SILURIAN.
Only at one point a series of strata was found to crop oat that might
be referred to this formation. Although no fossils were observed, and
the underlying formations had been thoroughly metamorphosed, the
overlying Devonian beds determine the view that they can be placed as
belonging to this formation. To the southwest of station 3d, in tbe
canon through which Lime Creek finds its way, a succession of sand-
stone strata were passed, to which the above remarks refer. It is a
white, coarse-grained sandstone, deposited in thick strata, that dip at an
angle of about ten degrees to the southward at the point where they
were seen. Owing to the densely- wooded character of that portion of
the district, no satisfactory data could be obtained regarding the dip at
other points. This sandstoucj which was observed at no other locality
310
"TOUCH. J DEVONIAN. 211
tbroagbout the entire district, has probably furaished a large portion of
the material to which the quartzites of that region owe their existence.
Lithologically it is so characteristic that an outcrop at any other place
mast necessarily have been identified with it ; and it is to be hoped
that the explorations daring the summer of 1875, during which time
the eastern limits of the metamorphic area can be studied more in de-
tail, will throw additional light upon its position in the geological scale.
DEVONIAN.
Of by far greater importance than the preceding isolated outcrop is
the area covered by Devonian strata. One feature adds greatly to tlie
interest of this group. It is the fact that at some points more exten-
sive deposits, in a vertical direction, are found than at others, both,
however, resting directly upoh the metamorphic rocks. In character,
both lithological and paleontological, the beds, although considerable
distances apart, agree very well.
Upon reaching the summit of the pass that leads from Baker's Park
into the lower valley of the Animas, a light-blue to grayish limestone
is observed, in positu^ dipping to the northward. It is very similar to,
if not identical with, the limited outcrop at the head of Cunningham
Gnlch, where it rests upon the shistose rock, and is covered by trachyte.
This limestone formation continues along the edge of the mountains,
descending into the caiion and keeping a coarse of outcrop approxi-
mately parallel to that of the Animas. Section II, given in the discussion
of the Carboniferous^ will show the position of the limestone with refer-
ence to overlying and underlying strata. Weathering in steep bluffs,
of no very considerable height, however, this rock presents a striking
appearance all along the regions of Lime Creek down to the junction of
the latter with Cascade Creek. Rhynchonella^ Spirifer^ and numerous
remains of Crinoids that are found at almost every point of exposure
facilitate the identification. For the entire series of strata at tbat lo-
cality, a thickness of 1,200 to 1,500 feet may be given. This, as will
be seen below, is by far more than the thickness of parallel beds at any
other point. Bat little variation in the lithological and stratigraphical
conditions takes place. Above the limestones the Carboniferous beds
begin, while they are underlaid, probably for a considerable distance,
by the Silurian sandstone. This was observed, however, only at one
point. It seems that the metamorphosing agent, that thoroughly
changed a large portion of the Devonian strata farther south, either
did not reach to the region that has jast been discussed, or that an
abundance of material underlying the Devonian rocks was suflicieut
to exhaust its force.
A second oatcrop belonging to this formation occurs immediately on
the southern boundary of the metamorphic area, running in a north-
westerly direction from station 48. This station is located on an iso-
lated patch of Devonian limestone, surrounded on all sides by metamor-
phic granite. Besting immediately npon this granite, which showed a
very marked stratification, conformable with that of the saperincum-
bent sedimentary beds, a white to red and brown qanrtzite was found.
At some points the contact of the latter with the granite was so inti-
mate that specimens could be obtained, showing both the granular
qnartzite and the coarse-grained granite on the same piece. No definite
relation of the colors exhibited by the quartzite could be established,
save the general rule that the nearer it was to the underlying meta-
morphic rock, the more intensely it was colored. Proceeding in a south-
212 GEOLOGICAL SURVEY OF THE TEBEITORIES.
"westerly direction from station 48, granite is crossed, and a sbort dis-
tance beyojid the same stratum is found, bearing the same relations to
over and under lying formations. It is evident, from the stratigraphical
character of the granite, and from the position it occupies with refer-
ence to the sedimentary beds, that at the place to which these remarks
apply, it was formed from sedimentary deposits that have now disap-
peared. Above the quartzite is a thin stratum of yellow siliceous
shales, containing narrow interstrata of softer shales. In these the well-
known and characteristic pseudomorphs after salt were found. During
the formation of the Devonian beach that now remains quartzite and
quartzitic shales, portions of the water, that even at so early a geological
))eriod contained sodium -chloride, were separated from the main body.
Ui)on eva{)oration the mineral constituents of the water crystallized. Sub-
sequent inundations of the places that had scarcely been laid dry, brought
with them sand and silt, covering the n«wly-formed crystals. By the
gradual percolation of water through the cover the salt was dissolved,
and a quantity of the material composing the cover found its way into
the cavities thus produced. It will be noticed, therefore, that whenever
these i)seudomorphs of sand after salt are found in positUj the crystals
will be observed on the /otrer side of stratum containing them. OcQurreuoes
of this kind are not uufrequeut in younger formations both of this
country and Europa Besides these pseudomorphs, scales and frag-
ments of bones are found, belonging to some fish of considerable size.
Too little material could be collected to admit of any i'^entification,
even only generically. Small scutellse also occur, probably belonging
to the same animal. This stratum, as well as the quartzite underlying
it, can be traced on the southern side of the granite strip.
Above this the limestones set in. On station 48 it presented a very
curious appearance. In every direction the isolated stratum is traversed
by vertical fissures, sometimes 8 to 10 feet in width, sometimes only a
few inches. Throughout the entire mass innumerable small cracks occur,
so thoroughly breaking up the limestones that it was a difficult matter to
obtain even small fossils that were not already broken. The whole
phenomenon was that of the result of a vertical force acting with lim-
ited lateral pressure. I ascribe it to the same cause that produced the
metamorphosis of the underlying strata. As in the two preceding cases,
this limestone also continues farther south, forming an abrupt bluft
toward the northeast and east. The continuation shows more strata
than were observed on station 48, but the horizon for fossils remains the ^
same. Here the evidence of decomposing and disturbing influences is not
so thoroughly marked, although it can readily be noticed. Thousands
of fossils were found on station 48 belonging to a few species only, but
nearly all of them in a very poor state of preservation, owing to the
causes above given. At some places the limestone was almost entirely
composed of the remains of BrtwhiopodSj while at others they were
distributed more sparingly. This stratum seems to me to mark the •
upper limit of the Devonian formation in that section of country, and,
although no very decisive paleontological evidence can be adduced for
assigning the overlying beds to the Carboniferous, it must be remem-
bered how very closely the organic remains of the Upper Devonian and
Lower Carboniferous are related to each other in our western groups
belonging to those formations. A number of s{>ecies were found in the
limeslone of station 48 and its continuation southward, which Professor
V. B. Meek has kindly identified. He describes, from the material sub-
mitted to him, a new species,* the description of which is given below.
*6n11etiii United States Geological and Geographical Sarvey, second series, No. 1, 1875,
page 46.
KDucH] DEVONIAN. 213
A suiall Prodiictm w^ts found, resembling P. subaculeaius ; oe<mr8
spariugly. Ortlioceras is found, but in a very poor state of preservation.
Athyris and Rhynchonella occur. Bellerophon and Euamphalus were col-
le(;ted in imperfect specimens.
By far the most numerous and varied species occurring there is the
one described by Professor Meek as —
Ehynchonella Endlichi, Meek.
•
Shell attaining a rather large size, subtrigonal, with breadth nearly
or quite equaling the length, the widest part being in advance of the
middle, becoming very convex with age anteriorly; posterior lateral
luariiins straight, or:but slightly convex in outline, laterally compressed
or flattened, and diverging from the beaks, in adult specimens, usually
at alK)nt right angles or less; anterior lateral margins rounding to the
front, which is generally more or less produced, and, as seen in a direct
view tiom above or below, transversely truncated or a little sinuous at
the middle. Dorsal valve very convex, particularly along the middle,
the elevation increasing rapidly to the front, which is raised so as to
lorm a very prominent, broad, rounded, or somewhat flattened, and
Klightiy-de fined mesial fold, rarely traceable back to the central region,
while, on each side, the lateral slopes descend abruptly to connect with
those of the other valve; benk moderately prominent, and incurved more
or letis nearly at right angles to general plane of the valves ; interior
with a prominent mesial septum extending forward nearly half way to
the front. Ventral valve flattened at the umbo, and so broadly and pro-
loandly sinuous from near the same anteriorly as to leave only a promi-
ueutaugular margin on each side, the sinus being broadly flattened along
the middle, and increasing rapidly in depth to the front margin, which
is carved npward more or less nearly at right angles to the plane of the
valves, and pro^luced in the middle, in the form of a large extension
fitting into a corresponding sinuosity in the middle of the front of the
other valve; anterior lateral margins on each side of the sinus meeting
tbo^ot the other valve at acute angles ; posterior lateral margins very
abruptly deflected and rectangularly deflected along each side of the
sinus, to meet those of the other valve; beak comparatively small.
Surtace of both valves ornamented by numerous radiating cost^e, which,
on the umbone^, are ^merely distinct raised lines, but increase in size
anteriorly, particularly those in the sinus and on the mesial fold, where,
toward the front of adult specimens, they become moderate-sized,
rounded ribs, of which four to six or seven may be counted in the imme-
diate flattened bottom of the sinus, and two or three more on the fold,
while those on the lateral slopes bifurcate, and continue, of smaller size,
to the anterior and antero-jateral margins. (Finer surface-markings
mikuown).
Length of an adult specimen, 1.78 inches; breadth, 1.53 inches; con-
^exiry, about 1.24 inches.
This is a fine s|>ecies, more nearly resembling some Devonian and
Upi>er Silurian forms than the usual Carboniferous types. Its most
piarked features are the large size of its mesial sinus, the flattening of
its posterior lateral slopes, and the angularity of the posterior lateral
niargins of its ventral valve on each side of the sinus, formed by the
abrupt flexure of those margins to meet those of the other valve. This
inflection of the posterior lateral margins gives this part of the shell a
pocaliar truncated, rectangular appearance, contrasting strongly with
the very acute angles formed by the connection of the antero-lateral
margins of the valve.
214 GEOLOGICAL SURVEY OF THE TERRITORIES.
The specific Dame is given in honor of Dr. £ndlich,of the United
States geological survey of the Territories.
Location aivd jMmtion.^— East of Animas River, Colorado Territory,
where it occurs associated with a small Produciua of the type of P. stdh
aculeattu. According to Dr. Endlich's sections, as well as from its
affinities, it would seem to be most properly of an Upper Devonian spe-
cies. Fragmeuts of it have been brought in from other localities in the
Bocky Mountains.
As mentioned before, the Devonian strata extend from station 48 in a
northwesterly direction, reaching nearly to the edge of a canon that
separates the main mass of the Quartzite Mountains from the sedimen-
tary area. A number of points along this line of outcrop are the high-
est on the sedimentary ridges. True to the general character of the
stratigraphy of that region, the beds dip oft' to the south aud southwestv,
at an angle varying from two to six degrees. So far as could be deter-
mined, the strata show very nearly the same condition in the other
portions of the Devonian area, as they were describe<l from station 4H.
A section taken from station 48 to station 49 (section 1,) which is located
on Lower Giirboiiiferous strata, will show the relations of the sedimentary
beds to the nnderlying metamorphics. Under the granite a shi^tose rock
sets iu, a, that is merely a continuation of the large masses occurring near
the borders of thequartzites. Above it follows the stratoid grauite 6,
dipping off to the south and southwest coniormably with the overlying
beds. The quartzite sets in then and continues to the southward, c.
Ascending higher, we reach the siliceous shales, c2, containing the psea-
domorphs of salt and the remains of fish. Blue limestone, «, forms the
capping of the small plateau upon which station 48 is locnted, and, as
well as the rest, continues southward, growing thicker, however. Above
this the Carboniferous beds set in. The entire thickness of the sediinen-
taries at station 48 amounts to about two hundred feet, while farther
south the limestone, e, alone reaches that figure. Horizons tor fossils^
that were observed alongthebluffssonth of station 48, let itap|)ear that the
stratum covering that point must ha ve been either eroded or must ha ve dis-
appeared in consequence of the activity that produced the metamorphic
rocks. Comparing the thicknesses we find here with those observeil on
LimQ Creek, the striking difference will be observed at once. A very
large portion of the Devonian strata has been converted into coarse-
grained grauite near station 48. I see no reason to assume that the de-
position at that point wa^ less in thickness than twenty miles farther to
the northwest. These two localities exhaust the out<5ro[)8 of Devonian
rocks in our district. Their relations to overlying formations are very
simple, having a conformable stratification.
CARBONIFEROUS.
Members belonging to this formation cover a great deal more gronnd
than those of the preceding group. It is mainly divided into two divis-
ions, the Lower Carboniferous, aud the Upper, containing the red sand-
stone. The former crops out all along the west side of the Animas, down
to about the middle of Animas Park, while on the east side of the Ani-
mas it forms a part of the higher ridges sloping off southward from the
Devonian area of that region. Throughout the area which it covers, its
stratigraphical relations conform entirely to those of the underlying De-
vonian rocks. Varied as the formation is, and notwithstanding its quite
considerable vertical development, but few localities were found where
characteristic fossils afforded any definite evidence legarding age. The
' I
Stazionu
Library,
Biouun.l CARBONIFEROUS. 215
absence of fossils was particularly noticeable iu the npper division, iu
tbe reel sandstones. With their aid, t. e., with the aid of typical forms,
aDy lingering doobt regarding their age could have been cleared satis-
factorily. As it is^ only a few organic remains were foand, and it be-
comes necessary to employ stratigraphical evidence in support of any
view that may be ent<ertained with regard to their age.
While the lower division of the Carboniferous is composed of a
series of beds, containing sandstones, shales, and limestones, the up-
per is confined almost entirely to the massive beds of red sand-
stone. In its lower strata the former shows mainly yellowish sand-
stones, interstratified with yellowish and gray shales, while, higher
Dp, the blue limestones set in, containing characteristic fossils. Imme-
diately above that the red sandstones begin, aud continue in an un-
broken series until the white sandstones of the Lower Cretaceous are
reached. Trias and Jura are missing or reduced to a minimum and only
exposed locally. Of one feature mention may be made, that had a
great influence upon the subsequent configuration of the country and
determination of the drainage. In the chapter on metamorphics an
anticlinal axis has been alluded to, running through a large portion of
the sedimentary formations, and continuing from there eastward through
tlie Qnartzite Mountains. So tar as our work extended westward the
traces of this disturbance could be observed. The line it pursues is
approximately from west to east, with a number of small curves. A
Hiiort distance west of station 37 it was first noticed, running a little
northward past that station ; it then makes a curve toward the south,
and croSvses over to station 36, from there over to Cascade Creek and
station 31, crossing slightly to the north of it; tbilowing the same
direction, it runs south of station 38, and enters the metamorphic area.
Its eastern termination seems to be lost under the trachyte, which
Kobseqnently invaded the region. On its north side the Cretaceous beds
on the San Miguel and Rio Dolores take no part in the dips produced by
the elevation along the line given. Toward the west the dips produced
are not so steep as those farther east. It can be seen, however that>
quite frequently the line of strongest upheaval is markeil by the courses
of creeks, the strata dipping oft' on either side from them. Proceeding
toward thequartzites, however, this changes. Some of the highest points
of that group show their metamorphosed beds dipping off on either
side of the summit to the north and souths The course of the an-
ticlinal axis is there marked by a n»w of prominent peaks, prominent
both on account of their altitude and the steep slopes they present.
Throughout the entire older se<limentary area, south of the given line-
its efi'ect can be recognized. Although the Cretace«>us beds dip off*, ap-
parently uniformly, in the same direction, uncontbrmabiiities were no-
ticed iu several instances, and it is quite probable, therefore, that their
dip is to be explained by a gradual rising of that portion which
then was land, rather than to be regarded as the result of the same
upheaval. The fact that volcanic material at numerous places covers
both the metamorphic and older sedimentary strata, resting uuconform-
ably upon them, shows that the disturbance must certainly have taken
place before the time of the volcanic eruptions. On the other hand, it
will be found that Cretaceous beds, appearing to have suffered no im-
mediate dislocation from the sanie cause, are likewise covered by vol-
canic rocks of the same age, so that the appearance of the latter upon
the surface could scarcely denote the extensive upheaval. Inasmuch as
all the Carbon if isrous beds we have in the district hare been affected
alike, it seems correct to conclude that the anticlinal axis in question
216 GEOLOGICAL SURVEY OF THE TERRITORIES.
<
was formed not very long after the deposition of the strata composing
that formation. As to the causes to which it owes its existence, I have
no explanation to oflfer, althou[?h I think it highly probable that its
occurrence is in intimate connection with the production of the meta-
morphic rocks, the formation of which certainly fell into some period
subsequent to the Devonian epoch.
Overlying the last-named formation, on the east side of the Animas,
we Mnd the Carboniferous beds. Analogous to those on the west side,
if not identical, they commence with a series of sandstones and shales
containing fragments of plants. Isolated interstrata of fossiliferous
limestones occur. Higher up the heavier limestone strata are reached,
and then follows the red sandstone. Referring to section I, given under
the head of Devonian, we see that there is a white, coarse-grained,
qiuirtzitic sandstone, <)f, deposited upon the Upper Devonian limestone.
This 1 regard as a good horizon to mark the beginning of the Carbouif-
erons. Above it follow yellow to brown sandy, shales, h, weathering in
small tabular fragments, attaining higher up more of the sandstone
character, i e., losing that of shales. Thin beds of limestone, contaiuiiig
corals, occur in the sandstones. Upon the next highest stratum, i, sta-
tion 49 was located, at an elevation of 11,700 feet. It is a dark-blue
limestone, containing Athyris suhtilida. Its thickness is not great,
amounting to 80 to 100 feet. It is covered by yellow sandstone, Z, in
which numerous fragments of plants, probably belonging to Uqmsetum^
were observed. Yellow to brown sandy shales, m, and marls follow
above this, underlying the red sandstone, n. Of this but little can
be said, inasmuch as its stratigraphical conditions are very uniform,
and the variations shown by its single beds but slight. Some of
the latter show more of a shaly character, in that case having a
darker color; others are more coarse-grained than is usually the
case. The thickness of all these beds will amount to over 3,000
feet, of which nearly 2,000 belong to the red sandstone. Station 40
is located ion this sandstone, toward the lower end of Animas Park,
on the ra^t side of the river. Dipping southward at an angle of
aliout 6^, it does not quite reach down to the valley, but permits
the underlying limestones and shales to crop out. Farther east they
seem to pinch out and are not cut by section I. Descending from that
station Athyria suhtilida Wds found m positu in a thin, shaly stratum
within the red sandstones, nearly one thousand feet above its
lower limits. A short distance below the latter, blue limestone set in,
containing numerous specimens of Prodnctus senmtriattiSj Athyris sub-
tilidaj and Spirifer. One Productus semistriutua was found on station
40. i. e.y in the highest third of the red sandstones. It'was not in posi-
tion, however, and although I cannot conceive of any plausible method
by which it might have been transported thence, I hesitate to accept
it as positive evidence. A short distance south of station 40 the sand-
stone reaches the valley, and the underlying beds are hidden from view.
The I hickness of the Carboniferous strata exposed at station 40 is ahout
eighteen hundred to nineteen hundred feet, nearly fourteen hundred feet
of which are formed by the red sandstone. The eastern limit of the
Carboniferous occurs near the Rio Vallecito and over toward Kio Pioos.
Owing to very dense timber, fewer observations could be made than
might have been desirable, but enough was seen to show that both ver-
tical development and stratigraphy remain unaltered. So far as could
be determined, none of the Carboniferous strata were altered by the ex-
tensive metamorphosis that took place farther north.
Ascending from Baker's Park the pass that leads into the lower val-
*
** • ^ . .
/^,
KKDUCR. ] CARBONIFEROUS. 217
ley of the Animas, at an elevation of 10,460 feet the sedimentary beds
are soon reached, beginning with the Devonian. Resting immediately
npon it are the Carboniferous strata, beginning again with the lower
series of sandstones and shales, in teratratified with limestones. Sonth
of Saltan Mountain (station 26, 13,306 feet high), the strata have a
soQtherly dip, both the Devonian and Carboniferous, while the overlying
trachyte covers them, nearly horizontally stratified. Proceeding from
that point to the southwest, toward station 31, it will be observed that
the dip changes into an opposite direction, producing a synclinal fold.
Upon reaching the station mentioned, however, it returns to such a posi-
tion as to become parallel again with the first. This latter change is due
to the influence of the main anticlinal axis that has been discussed
above. Engineer Mountain (station 31) is located upon an isolated i)atch
of trachyte superincumbent upon the red Carboniferous sandstones.
Although no very marked stratification can be observed in the volcanic
rock of that small peak, its direction is indicated by the vertical position
of the columns in which the trach.vte there weathers. The unconforma-
bility between the two is not so marked as farther to the northeast, owing
to the fact that the eruptive material is found almost directly on the
axis of upheaval. A clearer view of the respective relations can be ob-
tained from the accompanying section II. Starting from the northe{\8t,
the metamorphic rocks, a, are found to underlie the sedimentaries.
They are covered by Devonian limestones, &, containing numer-
ons fragments of corals and Spirifer, analogous to the rock upon
which station 48 was located. After that the Lower Carboniferous series
sets in, c, composed of yellow to brown sandstones and shales, inter-
stratified with beds of limestone, some of which contain Producfus semi-
striatus. Heavy beds of the red sandstone, </, follow, showing a very
considerable development of that formation. Toward station 26 these
are capped for some distance by trachyte, e, running out on the spurs
from the main group of mountains. To the north of station 31 a liine-
stone occurs above the sandstones, exposed on but a small area, and »f
no considerable thickness. The absence of characteristic fossils in these
strata is very much to be regretted. Crinoids and corals of a decidedly
Carboniferous type were found there; but such remains b^' which their
age could have been established definitely were not observed. Strati-
graphically they are conformable to the underlying beds. During the
smnmer of 1873, 1 fonnd in the red sandstones composing a large por-
tion of the JSangre de Ciisto range, near their upper limit, beds of lime-
stone that showed the same fossils. I am inclined to believe, therefore,
that these two may be parallel; all the more as I consider the sand-
stones of the two regions as being of the same age. Crossing that out-
crop of limestones, and proceeding northward toward the head of Bear
Oreek, we again descend into the region of red sandstone. All along
Bear Creek it forms the high slopes on either side nearly down to the
jnnction with Mineral Creek, dipping ofl' gently to the west. At that
point the thickness of the sandstones amounts to about 1,800 feet. Near
thejunction, erratic bowlders of the Lower Carboniferous limestones may
be found, originating from a small outcrop of those strata on the north
side of the creek. While the sedimentaries are thus found in the lower
canons, volcanic rocks form all the high points. On Bear Creek,
al>out two miles above the junction, a conglomerate may be observed
forming one of the highest strata of the sandstone group. Immediately
above it the trachyte begins. By the action of the latter it has become
thoroughly baked; is hard and well cemented. At no other point was
a conglomerate observed in the same horizon, and it seems probable,
218 GEOLOGICAL SURVEY OF THE TERRITORIES.
therefore, that it may have been a local formatioD. The high ridge
npoa which station 30 is located, dividing the waters of the San Miguel
from those of the Animas, shows a volcanic cap throughoat its entire
length. Grossing Bear Greek Pass, the red sandstones are again iboDd
on the west side of the ridge, althongh their horizontal distribntion is
limited. As on the east side, they are covered by trachyte, which shows
almost horizontal strata, slightly unconformable with the underlying
sedimentary beds. Here, aer well as on Bear Greek, the sandstones
show a number of white interstrata, a characteristic that can be ob-
served throughout, in the same horizon, along the exposures on the
Animas. Quite considerable metamorphosis has taken place in tlie
upper strata, produced by the overlying trachytes.
To the westward, opposite station 30, an interesting point may be ob-
served, where apparently the Garboniferous sandstones overlie the Greta-
ceous beds. This is one of the instances of unconformability alluded to.
The sandstones in question were deposited and raised* to their present
position, erosion had taken place and carved out much of the present
sha[)e, before Gretaceous waters invaded the region and the deposits of
Greiaceous Nos. 2 and 3 were formed. In the cafion north of station 36,
the sandstones again crop out, overlaid by Gretaceous No. 1. Farther
down on the Bio Dolores, they form both the bed of the river and the
banks on either side ibr some distance. In speaking of the volcanic area,
the isolated flows near stations 36 and 37 have been mentioned. The
fact that they do not stand in the same relation as regards time to the
preceding sedimentary deposits, receives an additional support, inasmuch
as tlie trachytes are found to occur, covering the Lower Gretaceous,
which rests in turn upon the sandstones of the Upper Garboniferous. A
number of cases were observed where the volcanic material is intrusive,
which shall be referred to below.
Near station 37, which is located on the red sandstone at an elevation
of 12,648 feet, this is the main rock, overlaid toward the north by the
Gretaceous beds, extending southward for a considerable distance.
About one-half mile north of station 37 the main anticlinal axis pa^^^ies
from west to east, producing a considerable dip, from 10^ to 18^, in
the strata. Either subsequent erosion, or a breaking of the strata, has
caused the small creeks of that locality frequently to find their courses
along the line of upheaval, whereas, in the quartzitic regions, the
steepest peaks owe their formation to it. A section taken through
station 37, in a direction of about north 30^ east (section III), will ex-
plain the stratigraphical conditions of the locality. The station itself
is located on a shaly stratum, 2», contained in the red sandstones, a,
From there the beds dip in a southerly direction, at an angle of about
120. Traveling northward, however, a depression is soon reached,
marking the line of the anticlinal axis, and from that point the strata
dip ofi' to the north. Numerous bluffs afford excellent exposures of the
beds, and the characteristic change of red and white strata is well cal-
culated to demonstrate the stratigraphy. Intrusive between the layers
of the red sandstone we find a bed of trachyte, /, apparently inter-
stratified, but pinching out, as the distance from the outcrop increases.
Two other deposits of trachyte were seen,/,/, the one capping a narrow
ridge, the other forming a small plateau. Both of them cover Gretaceous
beds. Immediately upon the red sandstones the white Gretaceous, No.
1, follows, composed of a fine-grained, hard sandstone, c. Whether or
not an unconformability exists there, was impossible to decide, as the
debris from the latter sandstone obscured the junction at all points
visited, and dense timber prevented any extensive view. Above No. 1
'TV-oAjie
f
//. '
\1
v '
93iXi
KDucH.; CARBONIFEROUS. 219
tbe gray shales of I^os. 2 aud 3, d^ follow, upon which the trachyte of
tbe small plateaa rests. From there westward the Carboniferous beds
crop out only in the lower country, while the higher shows Cretaceous
beds. This is the case also with the region lying north. An interesting
case of volcanic intrusion occurs immediately south of station 37, of
which section IV will give an idea. As stated above, the station ih
located on the red sandstones, a, which dip from there in a southerly
direction. Descending with them a stratum of trachyte, c, similar to
that described Irom station 36, is found imbedded in them, and after it is
crossed the sandstones again appear. Shortly after their first outcrop
has been passed, a trachytic dike, d, is reached, ascending nearly verti-
cally through the sedimentary beds. From there a small point is
ascended, and it will be observed that three other trachyte beds are
iuterstratified with tbe sandstones. Not far from the highest portion of
the hill a vertical fault has occurred, displacing the strata for the dis-
tance of about twenty to thirty feet. By this means the trachyte has
been brought immediately opposite the sandstones. It was noticed
that the volcanic beds diminished in thicicuess toward the south, some
of them pinching out almost entirely by the time they reach the opposite
side of the hill. A trachytic layer caps the entire series. From these
aud other instances where intrusion was observed, it would seem that
the eruption of that isolated mass of volcauics had been accompanied
by considerable dislocation, although the relative position of the latter
to tbe sedimentary beds precludes the probability of their having had
any share in the formation of the main anticlinal axis. Whence tbe
intrusive material came is a question that may require more study to
answer, but it seems to me, so far as I was able to acquaint myself with
the character of the geognosy of that section, that it must have pro-
ceeded from station 36. Both from stratigraphical and lithological
evidence I am inclined to accept this proposition ; all the more as the
Qiineralogical composition of all the volcanic rocks of that entire group
is a remarkably uniform one.
From the localities just referred to, the Carboniferous formation ex-
tends down southward for some distance on the west side of the Ani-
mas. All along the river, from some distance above station 39 down to
station 40, the lower division of the formation is exposed in the almost
vertical bluffs that border the Animas Valley on the west side. Litho-
logically the strata show tbe same characteristics that are exhibited on
the east side, and are, regarding the vertical distribution of beds, iden-
tical with them. Beginning again below with the series of yellow to
brown shales and sandstones, the bluffs rise to a relative elevation of
1,400 to 1,800 feet above the valley. Toward the top limestones set in,
containing some fossils. This formation extends westward and runs
lor some distance in a line approximately parallel to the course of the
Animas. It is soon, however, covered by the red sandstones. A num-
ber of mineral springs, alkaline, and containing soma iron, rise in the
lower division. One of them is situated opposite Animas City, near the
top of the bluff. Two more are found in the valley near the lower end
of Animas Park, starting at the base of the bluff. While the one is
cold, the other, but a short distance from it, is warm. A deposit, in
part calcareous, has been formed near them.
Resting upon these Lower Carboniferous beds we again find the red
sandstone, occupying, with reference to the former, the same position as
on the east side of Animas. Although there may probably be some
variation in the thickness of the beds, increasing as we go westward, it is
not of any great extent. A large area is covered by these red sand-
220 GEOLOGICAL SURVEY OF THE TERRITORIES.
Stones, extending from stations 36, 37, and 31 southward along the Ari-
uiosa, its western and northern tributaries, nearly to stations 42 and 43.
Densely timbered ridges, with only occasional exposures alongsteep banks
or bluffs, mark the horizontal distribution ot the formation under consid-
eration. The drainage cuts in deeply, leaving rounded spurs and ridges
to direct the future water-courses. Northwest of the junction of the
A imosa with the Animas, the first outcrop of the red sandstone near
the Animas Valley is observed. There it occurs as the capping of a
small hill, separated from the main mass, further «oath, by the cauon of
the Arimosa. About four jiiiles south of station 40, the sandstones reach
the level of the valley. From the northern limits of the sedimentary
formations, down to this point, they have preserved an even dip to the
south, varying from 4^ to 12P. At this point it amounts to about 5^.
As on the east side ol' the river, the sandstones show mterstrata of white
beds, arranged in the same vertical succession as there. There can be no
doubt as to the identity of the. formations on either side of thej river.
As soon as this point is established, it remains to be determined by
what agency they were separated, so as to give rise to the formation of
a broad valley between the two exposed walls. It has been nientione<l
of the Lower Carboniferous, that the blufifs it formed along the valley
were nearly vertical. A considerable amount of debris certainly ob-
scures the exposure of the face at the base, but presumably the same
general direction is continuous. This fact holds good also for the
red sandstones on one as well as the other side of the Animas,
luiismuch as the dip and strike of the strata are about the sameon both
sides, the former parallel to the general course of the river, and the
various beds reach the valley-bottom opposite each other, it is evident
that no disturbances took place by which both sides were not equally
afi'ected. Theagenciesby which thevalleyof the Animas could have lieeu
ibrmed are: (1) gradual erosion by the river; (2) glacial action of great
magnitude; (3) separation by contraction ; (4) separation by directly-iict-
ing forces. Gradual erosion by the river would certainly be the first to be
examiuedinto. There were evidences found, on stiition4<l, that at onetime
small erratic fragments, originating from the quartzitic group, were car-
ried alongatan eievationot nearly 1,800 feet above the present level of the
valley. It is possible, however, that they might have been brought by
some of the drainage flowing into the Animas from a northeasterly di-
ie(*.rion. This view is by far more plausible than that they should have
been carried there by the Animas itself. On the west side no such frag-
ments were observed. In case the valley had been formed by gradual
erosion, it would seem natural that those formations yielding most read-
ily to decomposing agents, should furnish the broadest portion of it.
Such, however, is not the case, neither in the npper nor lower pait of
the valley. In the chapter on metamorphics, mention has been made
of the evidences of former glacial action, and the granitic rocks in the
Animas Valley, resembling roches moutonn^esj near the head of the park,
have been alluded to. I am in doubt, however, whether the latter
owe their form to any action but that of gradual decomposition in
positu. We have, in this instance, a metamorphic granite, stratified to
so considerable an extent that the strata may easily be recognized, iu
addition to this, large crystals of feldspar are the predominating com-
ponent mineral, and the characteristic shape of this granite, now shown
at several points, can readily be accounted for, as the result of decx>in-
])osition progressing nnder circumstances thus favorable. Nowhere
throughout the region is there any positive evidence that the glacial
phenomena were anything but local, and of small extent. Separatiou
KDucn] CRETACEOUS. 221
by contraction would most likely have prodnced distarbances, eitber on
oue side or the otber of tbe river. No sacb disturbances were observed,
however. Tbe beds show no folding or dislocation from north to south.
Thronghout the region the gentle dip southward is retained. A num-
ber of facts speak for a separation by directly-acting forces. On both
sides of the river the formations are identical, and could the valley be
reduced to a line, the two rows of bluffs on the opposite sides wonld be
fonnd to correspond very closely. On both sides the faces of the bluffs
are nearly vertical, and there seems to be sufficient evidence that they
have been so for a very long time. The nearly straight course pursued
by the river since its* entrance intothe sedimentary country points to
the fact that the formation of its first bed was probably due to some
agent exercising a very considerable amount of force. Only through
tbe older sedimentary strata has thit^ force made itself perceptible, as
the river, after leaving them, is obliged to cut its own way through the
younger Middle Cretaceous beds.
About fourmiles north of the confluxof Junction Creek with the Animas,
the Ijower Cretaceous strata overlie the red sandstone unconformably,
which latter extends westward to the La Plata group. There it iscovered
by the trachy tic flows,which have their origin near the higher portions of
thegroup, and some of which extend overinto the Cretaceous area. While
the volcanic rocks are stratified nearly horizontally, the sandstone still
retains its southerly dip, thus producing an unconformability similar to
the oue east of station 31. The western limits of this formation were
not reached during our work in 1874, bnt will probably not be found to
extend much farther than the slope of the higher ridges.
A few isolated patches of the red sandstone occur in the northwest-
ern portion of the district, showing its considerable horizontal distribu-
tion. At the upper end of the creek, a tributary of the San Miguel, and
nqrth of which station 32 was located, it crops out covered by trachyti*,
which forms the higher portions of the ridge running from station 30
towards Mount Sneffels. I did not succeed in establishing to my own
satisfaction the relation it bore to the Cretaceous beds of that neighbor-
hood, but from all examinations that our limited allowance of time
enabled us to make, it would appear that it had been deposited and
placed into its present position before the Cretaceous waters reached
the locality. Another outcrop of the sandstone occurs in the Uncom-
pabgreca-non, about five miles westof station 10. Thecaiion is considered
inaccessible, owing to the precipitous character of its walls, the lower
portion of which belongs to the formation above named. Trachyte
covers it here as well as near station 32. With this the occurrence of
Carboniferous beds in our district is exhausted. They are very uniform
in character, and can readily be recognized, and although covering quite
a considerable area, show but slight variation in vertical development
CRETACEOUS.
This formation covers a considerable area in the district. Joining on
to tbe southern boundary of the preceding one, it extends southward
beyond the limits of our district, forming the characteristic low bluffs
of that region. Some of the highest points, where the Cretaceous was
found, show an elevation of 10,500 feet, while it reaches down below
6,000. As everywhere in Colorado, the single groups are well defined
and characteristic, both regarding their lithological and orographic
features. The southern portion, in Uie vfcinity of the Animas, resembles
more closely in the latter res[)ect the parallel groups of other localities,
222 GEOLOGICAL SURVEY OF THE TERRITORIES.
whereas tbe northwestern outcrops, along the San Migael, partake more
of the character of the western canon conntry. Single rklges, extending
for miles along the base of the older sedimentary mountains, impart
to the landscape that unique appearance, that has appropriately been
styled '^ Hog- back country." Small streams or rivers, cutting through
the ridges at right angles to their general trend, separate them into rows
of coffin-shaped hills, that generally have sharp crests, and regularly
sloping sides. Oak-brush and piiions comprise the greater portion of
tbe vegetation, rendering traveling a not altogether enjoyable enter-
prise. Wherever sandstones form the highest part of the hill, steep
slopes will be formed on the north side, by virtue of the southerly dip
the strata exhibit. Between the single ridges there is generally a de-
pression, sometimes amounting to nearly Sk) feet farther out into the
sedi mentary bluff conntry, of smaller dimensions, however. If the dip is
gentle, it becomes more so the farther the beds are removed toward the
south ; table-shaped bluffs are frequently formed, falling off steeply on
all sides, except the one parallel with the direction of the dip. As a
means for geognostic classification these ridges answer well. It will
be observed that the same strata, capping any one of them at a given
point, extend to either side without changing their relative position.
Differing entirely from the features shown in this region, are those of
the San Miguel neighborhood. Instead of the hog-backs and parallel
ridges, the Cretaceous there forms comparatively low ^' flats," rising on
the side toward the volcanic mountains. Deep cailons, frequently in-
accessible to animals, contain the rivers and streams. In them Creta-
ceous No. 1 is mostly exposed, while tbe succeeding higher numbers
overlie it, and form either gentle, grassy slopes, or are covered with
young growths of timber. After the mountainous region has beeo
passed, into which a bay of these Cretaceous beds extended, the bluff
character again appears. This, however, was beyond the limits set tor
our work during the season of 1874. Volcanic rocks overlie these sedi-
mentary beds at numerous points along the western border of tbe
trachitic area, and have occasioned considerable metamorphosis. Re-
garding the shape and distribution of the caOons, as well as the fiossible
causes of their formation, more shall be said in the course of this chap-
ter. Without a comprehensive knowledge based upon the observations
made over a very large extent of conntry, all conclusions must neces-
sarily be the result of an argument based upon insufficient premises,
and it will not be until the entire region has been carefully surveyed
and mapped, that questions of the cited character can be definitely
answered.
Cretaceous No, 1.
Without the appearance of either Triassic or Jurassic, we find the Cre-
taceous sandstones belonging to No. 1 resting immediately upon the
red Carboniferous sandstone. No transitory formations whatever are
in sight between the two, and I am inclined to think, therefore, that
tue Cretaceous waters of other regions invaded this, on the Animas,
while perhaps the land at the time was too high to be reached by those
of the preceding groups. From station 40, on the east side of the Ani-
mas, the bluffs opposite present a very good section, and it was from
there that the relations of the different series to each other could be
well studied. As shown in other sections, and treated of under the
heads of ^^ Devonian " and <^ Carboniferous," the sedimentary beds imme-
diately overlie the metamorphic rocks, dipping conformably with tbe
stratification the latter exhibit. Beginning with the Upper Devonian,
KDUC1I.1 CRETACEOUS NO. 1. 223
we pass, ascending, throngh the Lower Carboniferous, then through the
red sandstone, and about three miles north of the conflux of Junction
Creek with the Animas, reach the Lower Cretaceous beds. Up to that
point the dip and strike have been conformable, but as soon as the white |
sandstones, belonging to l^o. 1, are met with, a change takes place.
Although the general dip remains the same, its angle is changed to the
extent of (>o toS^. While the lowest strata show a smaller angle of dip
near the top of the hill on which they crop out, thej dip far more steeply
a short distance farther south. From the point above given, on the
western edge of Lower Animas Park, the lineof Cretaceous outcrop runs
along toward the northwest, the white sandstones always occupying a
position high up on the hill. They are white to 3'ellowish in color, mid-
dle to finegrained, sometimes stained in spots or stripes by hvdrated^
sesquioxide of iron. At stations 42 and 43 their most northerly limit^
is reached, and their elevated position tempted the Indians to use the
hills as ^Mook-out" points. From there northward nothing but red sand-
stone can be iound until the region of isolated trachytic eruptions is
reached. Almost due west of station 42, which is located upon a small
mass of trachyte capping these Cretaceous sandstones, is the La Plata
group, a portion ot whose volcanics covers the Carboniferous sandstone.
To the southwest from the station the line of Cretaceous outcrop con-
tinues, keeping ofl' some distance from the La Plata's. Very little varia-
tion is shown by the sandstones along the entire line of exposure. Below
they are massive, weathering in heavy, partly rounded bowlders; wher-
ever they form the capping of some blulf, and are of a more quartzitic
character they break into angular fragments. Remains of plants, that
cannot be recognized, however, on account of very poor preservation,
are found in them. Higher up the strata are no longer so thick ; and
after a thickness of 800 to 1 ,000 ieec has been passed, a bed occurs, show-
ing indications of coal. Immediately above these sandstones the shales
of Nos. 2 and 3 set in, producing, as a rule, a depression after the prom-
inent ridge of No. 1.
On the east side of the Animas, the conditions under which No. 1 oc-
curs are very much the same. It reaches the valley by virture of its
southerly dip opposite the point where it is reached by the same forma-
tion on the west side. The succession of strata is almost identical, with
this exception, that locally the indications of coal disappear. Inasmuch
as (heir presence is due only to particularly favorable circumstances,
this is by no means surprising, llere, as well as on the opposite side,
the white sandstones form the highest points of a series of hills border-
ing upon the Carboniferous strata. Toward the top, again, the single
beds become thinner, containing interstrata of shaly slates. On the
lace of the bluffs east of the Animas, the noncouformability was not so
stinking as on the west, but its existence is denoted by the difference
in the angle of the dip. A section taken from station 40, (Section V,)
in the direction of south 15^ west, past station 44, will give an idea of
the arrangement of strata. The lower strata given in the section be-
long to the older formations. Lower Carbouiierous beds are repre-
sented, a, overlaid by yellow shales containing strata of limestones and
sandstones, &, c, d. In these latter, Carboniferous fossils are found.
Above them follows a deposit of blue limestone, with numerous Pro-
ductus nemistriatusj 6, /, g^ immediately underlying the red sandstones,
A, upon which station 40 was located. One prominent stratum, of
white sandstone, t, middle-grained, readily decomposing, is noticed
among the red, while a uuml^r of smaller layers, less important, impart
to the steep bluii.a variegated appearance. Upon this red sandstone
\
I J- i '• r „ ,. „*'
\
/A
y
/"•*-*
■KWJCH.1 CRETACEOUS NO. 3. 225
at an elevation of 8,934 feet, T^hile camp 58, on the Florida, immediate-
ly below the station, is 7,530 feet. The shales of No. 2 have attained a
very considerable development here, and are covered by the yellow
sandstone, containing fragments of Inoceramus. For uearly a mile
along the northwest face of the very steep bluff, a series of ^' troughs" are
worn out in the shales, extending downward toward the stream. Nar-
row strips of the shales, from 80 to 150 feet high, separate the single
" troughs.'' Where the steepest portioh of the bluff ceases, these nar-
row strips show a bulging up of their ridges. Among themselves the
troughs are parallel and devoid of trees, except in the vicinity of the
stream. Probably they have been produced by snow-slides. An accu-
mulation of any considerable amount of snow in a region where the sun
has great power, even early in the season, could produce slides from
these steep bluffs that would readily accomplish the destruction of veg-
etation and give rise to the formation of these trough-like depressions.
In a horizontal direction the dip of the upper sandstone on these bluffs
varies. Instead of being almost due south, as that of the underlying
strata, it shifts to east of south on the east of the Animas, and toward
the west on the other side. The older sedimentary formations extend
southward in the shape of a wedge, and the younger ones dip off from
them, changing their strike, as the form of this wedge may require.
BidgeNo. 2 runs about 22^ south of west from station 47 toward the
Animas, and is then continued on the other side. Station 41 is located
upon a prominent point of it, 2J miles west of the river. A section
taken through station 47 (Section VI), running northwest to southeast,
will show the vertical distribution of strata. Below the Cretaceous beds
we find the red Carboniferous. sandstone, a, extending eastward from
station 40> Its dip is about 10^, a little east of south.
Above it appears Cretaceous No. 1, &, beginning with white sandstones,
of less thickness than further west; but the succeeding strata, o, com-
prising yellow sandstones and shales, show a better development. In our
section this forms the bed of the Florida. Traveling beyond the stream,
towards station 47, a low bluff is passed, the highest point of which is
formed by a yellowish sandstone, d, which closes No. 1. Here the dip
has already increased to about 18^. Above this the gray shales, a, of
No. 2 commence; first forming a gently-rising slope, then a steep bluff*,
which is capped by two strata of yellow sandstone,/, c; the lower one
is shaly, scaling off in thin plates, a.nd contains numerous remains of
plants, in a very poor state of preservation, while the upper is a com-
pact, fine-grained sandstone, weathering in rounded forms. It is the
one that forms the highest portions of ridge No. 2, and upon it station
47 is located. A depression occurs beyond this, occasioned by sandy
shales, h. Between this last stratum and the one preceding, coal is
found in some localities, but here none was observed. Overlying is a
bed of yellow sandstone, i. Probably this might correctly be regarded
as the terminus of No. 2, but discrimination between the two groups
becomes so difficult in this region that no positive assertion as to the
precise location of the boundary can be made. Then follow two beds of
yellowish to greenish shales, 2:, 2, the lower one darker than the upper.
A thick bed of yellow sandstone, m, forms ridge No. 3, upon which sta-
tions 44 and 45 were located, the former 3 miles east of the Animas, the
latter about 6 miles west. At the point where our section cuts this
ridfse, it is already of less prominence than further west. Higher up
in the sucx;ession of strata a series of light-colored shales, », containing
strata of limestones, o, occur, covered again by the same shales, p.
These belong to Cretaceous No. 3, and form very characteristic ^^ hog-
15 H
226 GEOLOGICAL SUBVET OF THE TERRITORIES.
backs," closely resembliDg tbose near Gafion City. From there the
Cretaceous beds begin to slope off very gently, forming low blnffs and
ridges for a considerable distance. Our work did not take us beyond
the third ridge. The comparative scarcity of fossils in the beds jast
mentioned is greatly to be regretted, because, with their aid, a more
strict classification of the strata could have been obtained. During ths
summer of 1875, in the continuation of the geological and topograph-
ical work in Colorado Territory, this region adjoining the south will he
explored, and more careful studies of the higher Cretaceous groups can
be made, than were permitted by the limited time and the plan of work
during 1874.
West of the Animas the ridges, that are no longer so prominent on
the east side, have retained their form and relative elevation. Station
45 is nearly 200 feet higher than station 44, both being located on the
same ridge, No. 3, but the latter being nine miles further east. From
there onward, however, the ratio of decrease is far more rapid. The
sandstone forming the summit of ridge No. 2 has given protection to
the underlying shales to so great an extent, on the west side of the
river, that a number of ^Hables " have been formed, similar in shape to
tbose produced by a cap of basalt on some readily-decomposing sedi-
mentary rock. On it is located station 41, south of Junction Creek. A
section taken through this station, in a direction of south 30° west, (Sec-
tion VII,) will give an idea both of the orographic features of the local-
ity, and of the vertical distribution of strata. Bed Carboniferous sand-
stone, a, again forms the lowest member of the section, underlying the
white sandstones, &, of Cretaceous No. I. Analogous to the variation
on the east si^^e of the Animas, a series of beds sets in, c dy comprising
sandy, shaly, and argillaceous sandstones. They already show an in-
crease in the angle of dip over that shown by the lower sandstone. A
yellowish sandstone, e, closes Cretaceous No. 1, immediately overlying a
bed of dark slaty shales, that show indications of coal. The gmy shales,
/, of No. 2 then follow, capped by the fine-grained yellow to reddish
sandstone of ridge No. 2. The ridges of this sandstone are not so reg^
ular here as some distance either to the east or west, owing to the fact
that frequently ** tables" wereformed,and subsequent erosion caused two
ridges to remain, Itoth capped by the same sandstone, A. Gray to green-
ish shales, t, corres|K)nding to k^ of section Y I, follow this sandstone.
This concludes the consideration of the Cretaceous area on the Bio
Animas and its tributaries. The formation varies but little in the ar-
rangement of its members from the schedule that has been long ago
established at other points, although in vertical development changes
occur even within short distances. One very interesting point was
studied here, the occurrence of coal. The conflicting opinions regarding
the age of coal-beds in a number of more easterly and northerly local-
ities are too well known to be dwelt upon, and it is a matter of impor-
tance, therefore, that its position here is established beyond dispute. In-
dications of it, and narrow seams, occur near the upper end of No. 1,
below the gray shales, containing Inoceramus and Oryphcea. Again, a
well-developed bed is found on the sandstone forming ridge No. 2.
Whether or not this bed is continuous throughout the entire formation
I am unable to say, but presume that where it is not actually developed,
indications will be found upon careful search. A third bed was found
by Mr. Wilson near station 45, the thickest thus far, resting near the
sandstone capping ridge No. 3. For miles beyond these ridges the Cre-
taceous beds continue in regular succession, sloping off gently in a south-
erly direction, so that no doubt as to the age of the coal cau be enter-
M
Q
O
22;
I
09
(7oa/ Indications
Library. )
I «
^ — •
Gray Shale g
Graff SKcde e [
mlvMlm// 1//MVM
7^ Yellow S€U9%dsiont
f Yellow S azideton^
d Yellow Sajidsto7i&
m//////\m
1i{//////M' l/////////A//^/.
0ly/////4l Ami<//A\S
tk y m - M ill y
'Xi^ht T/rowih Sandsto7i&
\//////il////m/4\4%i
. t P ! f
V
u
A ■■ A
Jl.
i
I
i.
T J
1
^
lU
■y
I
I.
1
T
r
-V — " V
I ■■ I
h
r
V y y
I_ — ^
looft.
\ WwU ScunxLstortd
BlMje Slates
Section Ym.
ODucfl.] CRETACEOUS NO. 2. 227
tained. It will be of great importance now to obtain the relation of
these beds to the coal-tearing strata further east, which will probably be
aciioiuplished daring 1875. By that meansthe two horizons, if there are
two, can be definitely located, and the question as to theage of the East-
em Colorado coal can be definitely solved. Mineralogically the coal is
a compact bitomiuons one, burning with fiame. Specimens obtained
were taken from the surface only, as neither time nor facilities were at
hand to go down upon them. Therefore any analysis that might be
given would furnish a result that could not be regarded otherwise than
erroneous.
Besides the Cretaceous formation in this region, it is developed on
the San Miguel and on the Bio Dolores.
Ascending Bear Creek up to the pass leading over into the San Mig-
uel region, we pass through the red Carboniferous sandstones. Tra-
chyte overlying them is next met with, and on the west side of the divide
the Cretaceous beds are reached. East of Moant Wilson, Cretaceous
'So. 1 appears in the canon of the San Miguel, and as its dip is in the
san^ direction with the course of the river, it forms its beds for a long
distance. On either side the shales of No. 2 form the soil, reaching
eastward to the trachytic mountains of the main group, westward to
the Wilson group, and to the north far beyond the limits of our dis-
trict. On the way to Mount Snefiels, we had occasion to traverse these
two Lower Cretaceous numbers, and to observe their contact with the
volcanic rocks. Camp was made on a creek flowing in a southwesterly
direction into the San Miguel, and there it was observed that all the
shales of No. 2, as well as the npi^er beds of No. 1, had been changed
by the action of the volcanic material. The former were thoroughly
baked and turned into hard slate, while the upper sandstones of No. 1
presented the apijearance of quartzites. In that region the Cretaceous
l)eds reach up into the narrow caiions, and are usually overlaid by tra-
chyte. In the vicinity of the rivers and streams, No. 1 crops out,
iorming the almost inaccessible canons through which they flow. A
section taken at the junction of the above-mentioned creek and Rio
San Miguel (Section YIII) will give some idea regarding the depth of
the caiions and the distribution of strata. It will be noticed that the
creek at which this section was taken has flown scarcely five miles,
and nevertheless the depth of its caiion amounts to 1,005 feet, accord-
ing to measurement. It seems, from the succession of strata, and the
fact that Inoceramus was found in the lowest one, that not the entire
No. 1 has there been developed. Beginning below, at the level of the
San Miguel, we find first 50 feet of dark-blue, partly shaly lime-
stones a, containing compressed specimens of Inoceramus. Above that
iollow 390 feet of white to light-yellow sandstones, fr, fine-grained,
and compact in structure, regularly stratified, having a straight dip to
the northwest, conformable with that of both over and unoer lying beds.
This is covered by 480 feet of light-brown sandstone, e, containing inter-
strata of greenish marls, underlying 40 feet of gray to yellow sandstone,
d^ weathering in grotesque forms. Above that follow a series of sand-
stone and shales, interchanging. The stratum mark hj in the section,
shows indications of coal, consisting of very narrow seams of jet, and
numerous coaled remains of plants. Above this the gray shales of No.
2 occur, with Oryphcea and numerous fragments of Inoceramus.
Although the question by what agents these comparatively deep
cafions were formed cannot be definitely decided, without a very thor-
ough knowledge of all their occurrences, the presence of those just men-
tioned, in a region so near the main mass of mountains, attracts atten-
228 GEOLOGICAL SURVEY OF THE TERRITORIES.
tion. It seems incredible that a stream should have been able to erode
a cafion more than 1,000 feet in depth, when the distance from its source
to the point of observation is bat tive miles, and it furthermore seems ex-
tremely improbable that such erosion should have progressed and the
walls of the canon have remained as steep as they are at present. I am
not prepared to defend any view on the subject at present, but it seems
to me that an effect produced either by volcanic or plutonic earthquakes
might have the same result.
About four miles below San Miguel Lake, the Lower Cretaceous sand-
stones set in in the canon, and continue from there as far as it was sur-
veyed. Crossing the divide from the San Miguel to Kio Dolores, the gray
shales are traversed. At that locality they dip off to the wesL The un-
conformability between them and the red sandstonesof CarboniferouAa^
has been mentioned in the chapter on Carbonitierous. From Moaut
Wilson the volcanic material has flown eastward, and covered a con-
siderable portion of the gray shales; at the junction they are somewhat
metamorphosed, but not to the extent observed in the region of Mount
Sneffels. To the south of Mount Wilson No. 1 again crops out, in the
canon of the Dolores ; along a number of the high ridges south oi the
river the characteristic white sandstones are found overlying the red
sandstones, covered in turn by volcanic rocks.
From the position the Cretaceous beds along the San Miguel and Rio
Dolores occupy, it is evident that they have been deposited at a time
long after the upheaval that caused the formation of the main anti-
clinal axis above mentioned ; and furthermore, it is very probable that a
considerable amount of time elapsed between the two epochs.
CHAPTER IV.
MINES.
The accompanying map was kindly prepared by Mr, Wilson, to serve
as an illustration for Balletin No. 3, second series 1875. By means of
lines running in different directions the geology of the region given has
been represented, and an explanation thereof will be fonnd bclow^the title
of the map. All the volcanic area, which has been treated of at some
length in chapter II of this report, has been left blank.
A number of the lodes visited during the summer of 1874 have been
indicated by heavy straight lines. Starting from the southeast corner
of the map, near station 17, it will be observed that the metamorphics
extend over from the quartzite mountains toward the volcanic area.
They are mainly schistose at that locality, containing a great deal of quartz
and some micaor chlorite. At several points their junction with the over-
lying trachyte can be seen ; forin8tance,atthenarr()wridgerunningsouth-
ward, about four miles east of the Animas. Although the connection
has been broken by overflowing tracb;ytic materials, the metamorphics
extend over into Cunningham Gulch, w1 ere they crop out. They form
the great canon of the Animas, below Silverton, that for a long time
was considered inaccessible both for man and beast. Another outcrop
of the same kind of rocks is found to the northwest of Handie's Peak
^station 14), where granite forms the lower portions of the caiiou lead-
ing down in a northerly direction from the mountain. The oldest sedi-
mentary strata that are found within the area given by this map are
the Garbonifeix)ns. Red sandstone, belonging to the upper group of this
formation, occurs first about one and a half miles west of the Animas,
unconformably underlying the trachyte that flowed from the north.
From there it continues west and northwestward^ and is exposed on
Bear Creek. A blue limestone is found covering it at one point north-
east of station 31. Cretaceous covers a considerable area in the west-
ern portion of the map* No. 1 is found in the deeper caiions, while the
marshy or grassy soil along the San Miguel is composed of No. 2. On
the banks of the Dolores and a few of its tributaries No. 1 crops out,
overlying the red Carboniferous sandstone, while it is covered in turn
by volcanic rocks.
At the time of my visit at the San Juan mines, August and Septem-
ber, 1874, but comparatively little work had been done. The greater
portion of the miners' time and energy was devoted to prospecting, and
but a few had then developed their lodes to any extent. One difficulty
under which they labored was the want of available capital, and of a
place where the ore might readily be converted into cash. It would be
impossible to give any fair estimate of the number of men scattered
over the country there, but I think that usually given is too high.
Mining is carried on at several points in the vicinity, and on tribu-
taries of the Animas Biver. Near its head, at the so-called '^ Forks," is
a complex of lodes (one of the early discoveries), and from it the locality
has received the name of " Mineral Point." Traveling down the river for
a distance of about six miles, Eureka Gulch is reached, another locality
229
230 GEOLOGICAL SURVEY OF THE TERRITORIES.
considered by the prospectors as very promising. A settlement lias
been made at Howardsville, on the Animas, this being a point more
favorable, perhaps, than many others, having the additional advantage
of being centrally located with reference to the mines. At the bend of
the Animas, near the base of Sultan Mountain, station 26, is Baker's
Park proper ; there is a settlement called Silverton. A short distance
to the east of Silverton is Arastra Galch, which became well known
some years ago by the discovery of the *' Little Giant '^ mine, and now
contains a number of others. In a similar position to Howardsville is
Cunningham Gulch, with a number of promising lodes, as yet compara-
tively undeveloped. Besides these points, prospecting and mining to a
small extent are carried on throughout the entire vicinity, both on the
mountains and in the caiions. Smelting- works were in the coui*se of
erection at Silverton when visited by our party, but, as I am informed,
were not completed satisfactorily.
Geognostically, the northern portion of the district just described
shows scarcely any important variation from the general character of
the surrounding country. All the rocks of that part, so far as I have
had occasion to observe, are volcanic, exhibiting, as at many other
neighboring points, a great variety in texture and mineral constituents.
From stations 13 and 14, the No. 4 of our schedule, above given, extends
west and southwest, changing in lithological character, although the
stratigraphical relations remain simple. I am inclined to attach con-
siderable importance to this latter feature, all the more so, inasmuch as
a satisfactory explanation of the geological relation could otherwise
only be obtained after very careful detail studies. The rock upon which
station 15 is located is of a grayish to muddy-green color, containing
small, irregular fragments of a triclinic feldspar,, and some sanidite.
Cubical pyrite crystals, of about 0.3™"* edge, are dispersed throughout
the rock, giving it, upon decomposition, a brown color.
Similar in general character, but varying in detail, are the rocks
composing the mountains on either side of the Animas down to Silver-
ton, and a short distance beyond. They are mainly aggregates, as
those from station 15, sometimes containing pyrite as an impregnation.
In Cunningham Gulch, the lower portions are of a dark-gray color with
a greenish tinge, while the higher portions of the hills bordering the
canon are capped by the bluish strata of the higher No. 4, as described
above from Handle's Peak. In Arastra Gulch the rock containing the
lodes higher up on the mountain-sides closely resembles that of station
15 at some points, while at others, without any great change in the
vertical direction, it answers more to the bluish variety. From all that
I could observe, however, I have come to the conclusion that the lode-
bearing rocks of Baker's Park belong to that trachyte series which has
been designated as No. 4.
This feature of regularity disappears when we study Cunningham
Gulch. Traversing the canon, whose walls rise 3,500 feet above the
creek, it will be perceived that the dark colors of the rocks still pre-
dominate, but that the lower portion of the steep walls has a tinge of
^ray and green, and is not horissontally stratified. This might, upon a
cursory examination, lead to the conclusion that the lower rocks, show-
ing weathering in a vertical rather t'jan horizontal direction, were co-
lumnar trachyte. A short distaooe below the. elevation at which the
*^ Highland Mary " and several other lodes are located, a sharply-marked
horizontal line may be observed, very slightly inclining toward the west
Above that line the rocks are horizontally stratified, varying from a
bluish to a maioon color — the trachyte No. 4.
KHDUCH.) SAN JUAN MINES. 231
Proceeding to the head of Cunningham Greek, the volcanic rocks are
seen only as forming the crests of ridges, while the main drainage runs
over metamorphic rocks. Station 17, near the head of the creek jast
mentioned, is located on gneiss, and may be regarded as one of the out-
posts of the metamorphic area already mentioned. From there the line
of outcrop extends east and southeast on the one side, west and south
on the other. Local accumuliMbions of mica or quartz change the lith-
ological character of the rock, and the appearance of chlorite in it gives
rise to a continuation of the metamorphic area to the southeast as chlo-
rite schist, the rock composing the lower portions of the Cunningham
walls, and containing a number of ore-veins. Farther down on the
Animas, where these metamqrphic rocks should be expected to crop out,
within a few miles beiow Baker's Park, on the Animas Caiion, we find
nothing but volcanics. Along either side of the river, from Cunning-
ham Gulch downward to the point just given, volcanic rocks appear to
form the entire mass in view. Although the lower portions of the rocks
exposed probably do not belong to No. 3, it is very difficult to identify
them with any one of the underlying groups, and they must be referred
to a position near to or in intimate connection with No. 4. Owing to a
large quantity of dSbtis in Arastra Gulch, the majority of lodes thus
far discovered have been claimed at an elevation of more than 1,000
feet above the creek. At no point in that gulch have I observed crop-
ping out of metamorphic schists, although I have reason to believe that-
they really do underlie the volcanic material. This suspicion is based
upon the character of the Little Giant ore, which contains chlorite and
none of the minerals mostly found in the trachorheites. Prospecting
has also been done farther down the river, but as my time was limited,
I bad no opportunity of visiting any of the lodes there located.
The conditions on the west side of the Animas appear to be of a more
simple character, the metamorphic rocks not reaching over in such a
manner as to crop out, although at some depth they may probably be
fbnnd. It is possible that considerable erosion took place before the
volcanic flows invaded the regions, and before the lodes were formed —
a view which is supported by the fact that near the head of Cunning-
ham Gulch a light blue to white limestone crops out, which, according
to its lithological character, must be referred to the Upper Silurian or
Lower Devonian of that region, no fossils having been found that might
establish its age beyond a doubt.
The metamorphic rocks of that region, in which stations 23, 25, and
38 are located, show many variations. From a pure quartzite they pass
over into micaceous schists, into gneiss, and at some points intoa coarse-
grained granite. Schists occur that contain the characteristic staurolite
twins, scarcely to be distinguished from some eastern localities. Nu-
merous small and large veins of white quartz traverse these schists,
showing sometimes slight indications of ore.
In speaking of the lodes of the region under consideration, it is nec-
essary to state that bnt little work bad been done upon them ; that
there are existing no mines of any appreciable depth ; and that but
very little time could be spent upon their inspection. These facta ex-
clude the possibility of deciding with any considerable degree of accu-
racy the character of the ore-bodies at any greater depth. It was nee-
cessary to make almost all studies on the immediate surface ; and as from
a series of such observations no law can be derived exhibiting the ratio
of development as compared to the depth, it stands to. reason that none
definitely to be relied upon can be here given. The geological char-
acter of the veins under consideration is a very interesting one, and I
232 GEOLOGICAL SURVEY OF THE TERRITOEIES.
believe that the data regarding^ development, with depth of the mineSf
must necessarily afford mach information on the distribution and for-
mation of ore-bearing veins in general.
OCCURRENCE OF LOBES.
Two systems, chiefly of lodes, are found, the one striking approxi-
mately northeast to soathwest, the other northwest to southeast ; and
the two directions may be observed to occur at the same places, produc-
ing a crossing of the veins.
At all points, where none but the volcanic rocks crop out, the veins
run through them in a very regular course, showing but few deviations
from the straight line. Often quartz veins, containing but little ore,
were observed from our high stations some distance ofif, keet)iug a regu-
lar course at times for more than a mile. As the quartz is harder than
the surrounding rock, it stands out prominently, while the former, imme-
diately adjacent, is weathered ofl'. Decomposing pyrite imparts a brown
color to the projecting ledge. As a rule, the walls may be pronounced
well defined, although near the surface atmospheric influences would
have the tendency to render them less so. Frequently the veins can be
seen along the face of a rocky hill for several thousand feet. This was
the case on a mountain opposite Howardsville, where a number of veins,
some of them claimed, are visible for a vertical distance of more than
2,000 feet. The accompanying cut will illustrate their position. From
the north side of the summit five parallel veins traverse the trachytic
rock for a yertical distance of 1,200 to 1,400 feet, and are in their turn
cut by a large vein starting ik'om the southern side, the ^* Mammoth lode.''
Farther to the south, beyond the last named, there are several smaller
veins, having an almost vertical dip. Debris covers the lower |K>rtion of
the veins, hidingthem out of sight. In Cunningham Gulch the lodes, after
first running through the metamorphic rock at right angles to its strike,
enter without apparent disturbance or dislocation the horizontally stniti-
fied volcanic cap. At the shallow depths which have thus far been
reached, no change in the character of the ore could be observed. The
stratification in Arastra Gulch is not so well marked, the rocks show-
ing a more massive structure, although a few miles beyond its head
they are regular again in their occurrence. Numerous other lodes al-
ready located occur in the volcanic rocks. The strike approximates to
that above indicated. No definite relation, however, of their course to
the structure of the rocks containing them could be observed.
Mineralogically speaking, the veins belong altogether to one system,
with the exception of a few in Arastra and in Bpulder Gulches, of which
mention will be made hereafter. Minerals of a relatively low degree of
volatilization form the main bulk of the ore, others, however, not being
wanting.
The persistency of the veins in a vertical di/ection is a matter of im-
portance, where nothing can be learned by the study of artificial depths.
It appears to me that it may be regarded as a rule that wherever
dibris or some, other similar cause does not obscui-e the view of the out-
cropping vein, that vein extends to considerable depths. About seventy*
five lodes were located on Mineral Point, showing very promising ore
from the surface downward. Sutficient work to retain the claim had
been expended upon quite a number of them. Several gentlemen, G.
W. Kingsbury, J. R. Hanson, A. W. Burrows, O. H. Mclntyre, all from
Yankton, Dakota Territory, and W. H. Van Gieson, P. Houghton,
and S. H. Tuttle, from Whitewater, Wisconsin, were continuing the
— HXTAlUrBHOUS VHHS KXPOSKD TO VIKW K
■TOUCH.] SAN JOAN MINES. 233
prospecting as well aa tbe fartber developments of tbe veins already
claimed. On Mineral Point tbe main strike is nortbwest to soatbeast
approximately, altbough several lodes cross eacb otber, and otbers
occar, striking from nortbeast to southwest. As a mle, tbe widtb be-
tween walls may be stated at 4 to 12 feet, bat larger veins occur. Tbe
ores mainly found are galeuite, middle to fine grained, containing
silver, sphalerite, from light yellow translucent to tbe brown varieties,
pyrite, cbalcopyrite, and fahlerz (brittle silver), which throaghout that
region appears to be an antimonial tetrahedrite, containing mainly sal-
pbur, antimony, copper, and silver, replacements being produced by
iron and zinc. About 8 to 13 per cent, of silver may be regarded as the
limits within which it occurs in tbe pure mineral. This variety of
tetrdhedrite has been distinguished as freibergite.
The gangne appears to be mainly quartz. As some of tbe locations
of that section, belonging to Bureka district, I would mention Dakota,
Mineral Point, Red Cloud, Little Twinkle, Mastodon, Bond Mine, and
£qnator. One of the lodes on Mineral Point shows a manganese de-
posit on the surface (psilomelane), while farther down galeuite forms
the main body of tbe ore.
In the Placer Gulch, Burrow's Park, Adam's Park, and at the head-
waters of the Uncompabgre a number of lodes have also been located,
showing ore similar to those from Mineral Point and tbe immediate
vicinity.
Upon tbe mines of Eureka Gulch no data could be obtained, owing to
a lack of time.
Descending Cunningham Gulch, Galena Mountain is found on the right
hand, while Kendall Mountain is on the left. Near the bead of the gulch
and on either side lodes have been located, and worked to some extent.
As above mentioned, tbe lower portions of the caflon consist of chloritic
schist, stratified, but standin gon edge ; while the upper portions are formed
by tbe bluish volcanic rocks of No. 4. Several well-defined veins extend
frnm the lower to tbe upper, and, as I was informed, the continuation
bad in two instances been traced beyond the ridge of the mountain to
the otber side. A considerable amount of debris precludes the possi-
bility of following the veins to the bottom of the gulch, but, judging from
analogy, they may be considered to extend some distance farther down
beyond the point where at present they can be seen. This cation now
being one of the main routes of ingress and egress to and from How-'
ardsville, prospectors bave been attracted more particularly to tbe
stady of its vicinity, and ore has been obtained from several veins,
yi< Idiug, even when taken from tbe surface, a comparatively large
percentage of silver.
Near the head of the gulch, on tbe left hand descending, the
HIGHLAND HABT
is located. It has a strike of north 68° west, and vertical dip.* Between
walk the gangue and ore average from 4 to 5 feet. To the northwest the
extension of tbe vein has been found and claimed as the '' Robert Bruce."
Toward tbe gulch the Highland Mary runs through the horizontally
stratified trachytes of No. 4, corresponding in character to that de-
ficribed from station 14, of a bluish color. The line of junction between
this volcanic rock and the underlying metamorphics is well marked and
readily distinguishable. Without showing any change in course or widtb,
* The dips are given as the variation from the vertical. •
234 GEOLOGICAL SURVEY OP THE TERRITORIES.
except a slight deflect Lou of about 3 feet, formiug a carve at tbat point,
the lode cau be traced downward through the schista for more than 2i)0
feet in a vertical line. These schists are of a greeu color, weatheriug
very dark. Quartz and chlorite constitute the two predominating min-
erals. Pjrite occurs scattered through it. Structure is slaty, with small
veins of quartz traversing at right angles to the plane of the schists.
After that debris sets in, and it would require some tunneling or other
work of a similar nature to reach the vein. Galeuite, intimately asso-
ciated with fahlerz (tetrahedrite), at many points forms the main body
of ore, and pyrite, sphalerite, andchalcopyritearenot wanting. Quartz
mainly composes the gangue. The ore occurs in seams, from the thick-
ness of a needle to 9 inches, without, however, showing any symmetry- of
arrangement. No further ^work had been done at the time of my visit
than the uncovering of a number of points along tbe vein, in order to de-
monstrate the continuation of ore. It is claimed that the extension to
the southeast across the canon has been found, but I did not visit the
locality.
THE ROBERT BRUCE,
as above mentioned, is the northwestern extension of the Highland
Mary, keeping nearly the same course. It has been prospected for some
distance, and the character of ore appears to vary but little from that
found below, although the distribution of the several minerals may not
be the same.
THE COMSTOCK LODE,
formerly called the Mountaineer, is situated on the same hill, about half
a mile nearer to the head of the gulch, and south of the Highland Mary.
Its strike is a more westerly one— north 75^ west. As far as could be
observed, it runs entirely in the blue trachyte. It may be, however,
that the downward continuation is merely obscured by dSbriSj or rather
large masses of broken rocks. Between walls it is on an average 4 to
5 teet wide, and has a slight dip to the south. Very little work has
been done on this lode, and mainly surface-ores, consisting of galenite,
,pyrite, &c., have been obtained.
THE YRETEVi.
is located opposite the Highland Mary, on the east side of the gulch.
It strikes a few degrees more to the west than the latter, and has the
schists as wall on either side. Farther down the caiion, on Green Mouut-
•ain, the
GREEN MOUNT Am LODE
»is situated, striking almost north 45^ west. Lower down it runs
tthrough the schists, cutting the strike of the latter at an angle of about
80^. It continues upward through them, and enters the trachyte,
without showing any perceptible change of course. The ore of all the
lodes in Cunningham Gulch is of the same mineralogical character,
notwithstanding the quantity and distribution of each specific mineral
may frequently vary.
THE PRIDE OF THE WEST
is also located on Green Mountain, and has an approximate course of
north 45^ west. Though it cannot with certainty be said to reach down
ETOUCH.] SAN JUAN MINES. 235
into the schists, this yet appears very probable. Three hundred feet
above the Pride of the West is the Equator ; 150 feet below, the Astor ;
both ruuning nearly parallel with tbe iirst.
Besides these, there are a number of otber lodes on the Cunningham
already claimed, but it was impossible to obtain notes on them all, inas-
much as the inspection of each would require nearly an entire day.
This latter fact is owing to the distance at which the mines are located
from any available camping-place, and from the fact that, besides be-
ing far apart, they are uiostly at a considerable elevation above the
creek.
We have on the (3unningham a series of silver lodes, wliich, so far as
surface-indications may be relied upon, do not change the character of
their ore when leaving the one and entering the other geognostic forma-
tion. At another locality, of which mention shall presently be made,
veins containing gold-ores are found. Higher up the mountains veins
appear, carrying very small quantities of tbis metal, but showing spe-
citic silver minerals.
In Arastra Gulch, about two and a half miles down the Animas from
Howardsville, at the mouth of Cunningham, gold-miniug was carried on
first. The gold was washed out by various methods, until the '^ Little
Giant " was discovered. This discovery led on to prospecting, and after
some time a large number of veins had been found and claimed. In
former times t he settlement there was one of good promise. It decreased
after the abandonment of gulch-mining, but, under the influence of these
Dewlydiscovered silver lodes, is again reviving. Although I spent as
uucb time as I couhl u\>ou the decision of the question whether tbe
metamorphic rocks underlaid the trachytes containing the lodes, I
could find no point where a satisfactory outcrop occurred. Judging,
bowev*r,fron) the close proximity of these rocks, Irom their trend toward
tbe region under consideration, and from the fact that the ore of the
Little Giant is associated with chlorite, being one of the lowest mines in
tbe gulch, I think it bighly probable that they do extend through^ and
that tbe veins probably run into them. The veins observed on tbe
bigber iM>rtions of tbe mountains forming the walls of the short canon run
in trachyte, belonging to No. 4, and have as a rule a course of east 10^
to 50^ south. A number of veins occur that vary from this, but tbe
niiijority preserve a parallelism among themselves. At the same time
they show no material deflection from the course of neighboring veins.
THE LITTLE GIANT,
as stated, is a gold-bearing vein, situated on the northeast side of
Arastra Gulch, with a course of about north 40^ west. It it well known
as one of the oldest mines of the region, and has yielded profits. A
tunnel is driven in from the southwest, striking the lode. A short
distance from the mouth of this tunnel crushing- works have been erected,
crashing the ore to a powder, and as such it is then treated by amalga-
mation. Central and Dexter are two gold-mines east of the Little
Giant.
On the opposite side of the creek, HazeUon Mountain rises to a
relative elevation of 3,600 feet, and it is upon the north and northeast
face of this mountain that a number of lodes are located.
EXCELSIOB LODE.
Upon this lode more work has been done than upon most others. A
shaft 30 feet in depth was smik, and a quantity of ore taken ont^ now
236 OEOLOGICAL SURVEY OF THE TERRITORIES.
formiug a sinall damp at tbe month of the shaft. Its course is east
390 south, and the width between walls 3^ feet. On either side tbe
walls, even at that slight depth, are well detiued, and composed of tra-
chyte, belonging, as in Cunningham Oulch, to No. 4. Tbe ore mainly
consists of galenite, middle to fine grained, sphalerite, pyrite, chaloo-
pyrite, and lahlerz, almost identical with the tetrahedrite mentioued
above.
THE PROSPECTER
is another lode, near the preceding one, having a strike of east 3P
south, and a dip of 18^ to the southwest. Wall-rocks on either side
are the usual trachyte, and the ore analogous to that of Excelsior.
THE PELICAN LODE
has a course of east 54^ south, with a dip of 15^ to the southwest
Two shafts of 18 feet each have been sunk upon tbe lode. For 1,500
ffet tbe outcrop has been followed and uustripped. Among a number
of other lodes that might be mentioned are McGregor, east 36^ south,
with a dip of 3(P southwest^ Aspen, east 55^ south, having reached a
depth of 40 feet ; a shaft sunk on the lode; Pathfinder, east 30^ south;
curving a little southward in its course.
A tunnel has been driven from Arastra Gulch sonthwestward into
the north face of Hazelton Mountain, with a view to cutting some of the
lodes cropping out on the surface. Work is being pushed at the above-
mentioned mines, although but few hands are being employed. The gen-
eral character of ore is similar to that of the Cunningham mines, with tbe
exception of those located lower down in the caiion. Other lodes are
located in different portions of the gulch, but I had no opportunity to
visit them.
Boulder Gulch is situated opposite Arastra, on the north side of tbe
Animas, and contains one lode, the Crystal, that shows gangue-rock
very similar to that of the Little Giant. In so far as this can be taken
as an indication regarding the possible presence of the schists at some
depth, it is important. Gold is the main paying metal in tbe Crystal.
Several localities occur, besides those mentioned, where prospecting
has been done and lodes have been opened.
On G(K)dwin Creek, about seven miles above its junction with Lake
Fork, a number of veins have been claimed, and ore was taken out. On
the 15th of June, 1874, the
Bia CASINO
was located at that point on the south side of the creek, and a shaft
sunk. The vein runs entirely in trachyte, w*hich is thoroughly impreg-
nated with pyrite. Ore has been found from the surface down, eom«
posed of galenite, sphalerite, pyrite, and fablerz. The ganguerock, as
usual, is quartz. On the other side of the creek, the
OXTELAY
is situated, yielding ore of the same character, running in the same
rock. Both lodes have good walls, and are worked for silver.
Near Baker's Park, on Mineral Creek, about four miles west of the
park, is the Silver Court, having a strike of about north 80^ east. It is
situated approximately at 1,000 feet above the creek, and shows tbe
usual ores of that region.
] SAN JUAN MINES. 237
It may be of interest to meDtion that near Lime Greek, some distance
down the Animas, proceeding from Bakei's Park, prospecting has
l>een done for chloride-ores, in the Devonian limestones of that region,
altbongh without any decided success. Almost all the mountains in
tbe immediate vicinity of Bakei^s Park, and the regions north of it,
contain veins ; frequently, however, without the remunerative metals.
They have been found of almost incredible width, and extending, well
defined, for miles. In a country where so large an amount of mineral
substance is present as in that which formed the field of our labors dur-
ing tbe summer of 1874, it cannot be astonishing that veins or even ores
should be found at any place where the conditions for their segrega-
tion and accumulation were in the least favorable.
Owing to the rugged character of the country, to the sharply-cut
avails, inclosing canons of considerable depth, and lastly to the regularity
of tbe veins in course and dip, mining can be carried on at compara-
tively slight expense should the veins eventually prove as remunera-
tive as their surface indications might justify us in presuming. A well-
re^ilated system of sinking shafts and driving tunnels, either to or on
the same vein, wonld afford facility for the regulation of water and air,
as well as for the first transportation of ore, that ought not to be over-
]ooke<l. Frequently the same vein can be taken, in work from above
in a vertical direction, while 1,000 feet below a tunnel driven will
afford tbe facilities above indicated, besides furnishing valuable iuCor-
ination as to the constancy of the ore, both in character and distribu-
tion. Timber exists in sufficient quantities to la«t for many mines.
One unfavorable circumstance is the short duration of the season dur-
ing which active work near the surface can be accomplished. After the
mines have reached a certain development, however, so that their interior
will be but little affected by the outside influence of atmospheric changes,
a great portion of this trouble will be obviated.
In summing up all that has been observed during the short time that
could be allowed for investigation of this interesting mining-region, it
becomes necessary not to overlook the difficulties that had to be over-
come. Above all, the fact that all the mines were but in their infancy
will tend to cast a shadow over the conclusions that may have been
drawn with reference to many important features. In consequence of
this fact, no reliable data with reference to the vertical distribution of
the ore can be given, and, although outcrops along uumerons points of
any lode may everywhere show favorable indications, nothing but a
future development of the new mines can disperse all doubt. Eegard-
ing tbe persistency of the veins in a vertical direction, a sufficient num-
ber of observations have been made to lead to the conclusion that their
general character in that respect is satisfactory. The ores contained in
the veins are of such composition that they will ofl'er no serious obstacles
in any smelting establishment that may be founded upon principles that
are not totally at variance with chemical and physical laws.
Geologically, the veins of our district are very young, probably having
been formed at tbe close of the Cretaceous or the beginning of tbe Ter-
tiary period. The enormous eruptions of the trachy tic lava, covering a
continuous area of more than five thousand square miles, must have
taken place at tbe geological period above indicated. In the beginning
of this paper particular stress was laid upon the impregnation with
mineral matter of certain volcanic strata — a phenomenon that occurs
over a large t^act of country. This shows that at tbe time of the
eruptions such conditions existed as were favorable to the formation of
that class of minerals generally termed ores. It is furthermore to be
238 GEOLOGICAL SURVEY OF THE TEEKITORIES.
observed that theee impregnations occnr mainly in the younger strata.
Althoagh the inference cannot be drawn that the fissures were formed
at the same time, or shortly after the deposition of the trachyticlava,it
is allowable to assume that at such a period the material for tilling these
fissures was existing near the locality where but lately so thorough an
impregnation had taken place. The fact that the fissures extend, at a
number of points, downward, through the older metamorphic rocks,
makes it improbable that they should have been formed by contraction
of the cooling masses. Singular as it may seem, these lodes are devoid
of that ore which is generally classed rs surface ore. Immediately from
the surface the perfectly fresh minerals are taken out. The gangue is
hard and solid. An exception is made, of course, although only to a
slight extent, by pyrite, which decomposes very readily when exposed
to the action of atmospheric influences. This characteristic may be
explained in various ways — by the rapid decomposition and breaking off
of the wall-rockS) carrying with them portions of the gangue and ore; by
the less intense eifects of atmospheric agencies; by the character of the
minerals composing the ore, and by the comparatively short time that
these fissures have been filled. The latter view is the one that would
to me appear as the most acceptable.
A difficult question arises, when a decision is to be made, as to the
causes that have produced the formation of the fissures that were after-
ward filled. Accepting, as I have always done, the theory that vol-
canic or plutouic earthquakes have probably produced the larger num-
ber of all lode systems — and such we have in this case — it will be neces-
sary to find whence came the requisite force. Along the highest por-
tion of the Quartzite Mountains we have an anticlinal axis which can
be traced westward for nearly forty miles, an upheaval that must hare
a very perceptible efiect on regions adjoining. The idea at first pre-
sented itself that this might have given rise to the formation of the
fissures, but evidence subsequently discovered demonstrates that long
before the eruption of the trachyte this disturbance had occurred.
About twenty miles west from the center of the mining region is a
series of isolated groups of volcanic peaks. The highest one of these,
Mount Wilson, reaches an elevation of 14,285 feet above sea-level,
about 5,000 feet above the valley. Lithologically these groups must
be considered younger than the lode-bearing rock of the Animas, and
must, therefore, have become eruptive later. It seems quite possible that
the disturbance produced by these eruptions may have resulted in the
formation of the present fissures, which subsequently were filled from
that source which supplied so much mineral matter to other neighbor-
ing rocks in the form of impregnation. It is extremely difficult to de-
cide questions of this kind, involving so many different factors, after
having made any but the most complete investigation into the subject
I therefore only offer this explanation as a suggestion, without any fur-
ther elaboration.
CONCLUSION.
lu the district which has been considered in the above pages, we have
a comparatively regular arrangenieut of the various geological forma-
tions. A continuation of the volcanic area first observed in 1873, has
been examined, and its southwestern borders liave been determined.
Adjoining that on the south is an extensive metamorphic region. Flank-
ing both the south and west are the sedimentary formations. Al-
though it is impossible in this case to retain any but the general ontlines
of a classification heretofore used in the determination of volcanic rocks,
we are nevertheless enabled, by the regularity of occurrence, to parallel-
ize them to a certain exteut. It is a notable feature that the eastern
portion of the volcanic region is the older, while the western — the higher
one — is younger. In connection tBerewith, probably, is the fact ob
served that all outcrops of strata covered by the volcanfcs are un-
changed sedimentaries in the eastern, wbile theyaremetamorphicsin
the western portion. This fact alone would, probably, prov^e to be a-
8troug argument in favor of searching for the point or points of outflow
iu the we|tern region. Considerable change in the niveau of the coun-
try must nave taken place, to which allusion has been made in chapter
li. Although so many features of interest are presented at almost every
locality of the area, the larger portion of it, i)robably, centers in the
mining region. We have there the case of ore-veins of certainly Post-
Cretaceous age, traversing old metamorphic rocks, passing through them
and entering the volcanic beds that are regarded as Tertiary. Too lit^
tie is known as yet of the vertical distribution of ore in these veins to
admit of any generalizations on the subject, but it seems probable that
characteristic features regarding occurrence and frequency of the differ-
ent minerals constituting the ores will eventually be observed. The
regularity and uniformity in most characteristics that these veins pre-
sent, the rarity of dislocations or faults, point to their having been
formed either at or very nearly the same time. Since making the ex-
aminations in Baker's Park, the mining district of Lake Fork has been
more fully developed, and the discovery of a limited number of lodes
has been followed by many others that show fair indications of satisfac-
tory results.
Difficult to study as the center of the metamorphic area may seem,
sufficient evidence has been obtained near its borders to admit of a
reasonable explanation of their origin. It appears that the entire Silu-
rian series, and at many places a portion of the Devonian have furnished
the material for their formation. Pure sandstones would then produce
the quartzites that have given the name to that prominent group of
mountains, while other rocks with more alumina, magnesia, &c., account
for the granites and schists. Were it possible, on account of time and
the rugged character of the country, together with its superabundance
of rain, to make the requisite detail investigations, I think the question
might be fully solved and much applicable information gained.
Mention has been made of the glacial phenomena observed in the
Quartzite group. Although they are limited to small areas their influ-
ence on shaping the drainage, and, by changing the surfaceof the ground,
producing 1akes*and swamps, has been quite considerable.
More varied in its single members than the preceding group is the
sedimentary poition of the district. Stratigraphically it is quite simple.
239
240 GEOLOGICAL SURVEY OP THE TERRITORIES.
A few local disturbances occur, but besides those only the great anti-
clioal axis is an object of interest. Although the Cretaceous beds of
the southern and western portion have the same general direction of
dip as the older ones, several localities have furnished evidence tbat
the disturbances affecting the Devonian and Carboniferous must have
occurred betore the deposition of the Cretaceous. It is possible that
to this fact, to the higher relative position at the time, the absence ot
Triassic and Jurassic beds may be attributed.
Begarding the different members of the older sedimentary formations
much might be said about their mutual affinities. The highest Devonian
has a decidely Carboniferous aspect, while, on the other hand, the lowest
Carboniferous shows affinities to the Devonian.* I have considered it
best to draw the line of distinction there where we have character-
istic fossils to aid discrimination in the future. Of the red sandstone
referred to the Carboniferous mention has often been made in the pre-
ceding pages. Based mainly upon stratigraphical evidence, wbicb, it
is true, is supported by meager paleontological proof, I regard that
series of sandstones as a member of the Upper Carboniferous formation.
It is, so far as I am able to determine, the same that in 1873 I distin-
guished as Arkansas sandstone.
During the coming field-season (1875) I hope to see more of this group,
and may succeed in establishing its age beyond doubt.
Some doubts have arisen as to the classification of the Cretaceous beds
in the southern portion, along the Animas. Inasmuch, however, as I
have not yet seen the entire series there, and will probably have occa-
sion to do so during the next field-season, I shall postpone the dis-
cussion of this subject.
* Compare : Report Uuited States Geological and Geographical Survey, 1873, page 34L
EEPOET OF SAMUEL AUGHEY, Ph. D.
16 H
241
I
i
THE SUPERFICIAL DEPOSITS OF NEBRASKA.
By Samuel Auohey, Ph. D.
The casaal observer, passing over Nebraska, little saspects the mar^
velous histories treasured up in the rocks beneath his feet. These nn-
derlying rocks represent foar great divisions of geological history. Gom-
mencing at the southeastern part of the State, and going westward
and northwestward, these divisions are, Upper Carboniferous, Per-
mian, Cretaceous, and Miocene and Pliocene Tertiary. The reader is
referred to the geological map found in Hayden's final Beport on the
Geology of Nebraska, for the boundaries and extent of these deposits.
In Hayden's reports will also be found the descriptions of these deposits
and the story of the extraordinary life of past times which they unfolds
The purpose of this paper is only to give some of the prominent fea<
tnres of the surface geology of the State ; and, therefore, the older rocks
are only referred to in the case of the Miocene and Pliocene dei)osit8,
where they constitute the surface in the bad lands in the northwestern
corner of the State. Nebraska owes the peculiarity of its surface and
its great fertility mainly to three deposits, namely, the Drift, Loess, and
Alluvium. The poorer portions are principally produced by the sand*
hills, bad lands, and alkali lands. These deposits will be considered
in the order mentioned.
THE DRIFT.
The Drift is the most widely-diffused geological deposit in the State.
It constitutes the surface-soil in some places, but generally it is found
directly below the Loess. In rare instances it seems to have been re-
moved from the uplands by denudation before the Loess was formed.
Sometimes where it is exposed at the surface it is so mingled with the
Loess, Alluvium, and organic matter as to escape the attention of any
one save a practical geologist. It ranges in thickness from a few inches
to seventy-five feet. It may be much thicker, but if so I have seen no
exposures that indicate it. Nowhere does it come to the surface over
wide areas. In the northern part of the State it occasionally constitutes
the surface, in the southern part of Dixon County, in the northern part
of Wayne, and in portions of Cedar, Knox, Pierce, Antelope, and Holt
Counties. In townships 30 and 31 north, range 1 and 2 east, in Cedar
County, semicircular rows of Drift pebbles and bowlders even yet extend
across narrow valleys, that lie on the flanks of high bluffs in the form of
terminal moraines of glaciers, the marks of which unnumbered
centuries have not been able to efface. In this region some ot the gla-
cier-marked bowlders are of great size, weighing many tons. One of the
most remarkable lies near the quarter-section stone, between sections
25 and 36, in township 30 north, range 1 east. It lies on
top of the highest bluff in this region, from which there is a mag-
nificent view of the whole country around. It is a granitic quartzose
rock, about four feet square. On the level top-surface there is a beau-
tiful engraving of a child's foot, a half-moon, a grape-vine, and other
.243
244 GEOLOGICAL SURVEY OP THE TEERITOKIES.
hieroglyphics. The engraving of the child's foot is cut in its deepe.^t
)>art, three-foarths of an inch into the hardest rock, and for fidelity to
nature it would do honor to the work of a Greek artist. Previous to my
discovery ot this relic of the past (1869), no one in that region had
heard of its existence. It may have been the work of the mound-build-
ers, as their peculiar pottery and mounds are found near by, but what
implements enabled them to carve these symbols in this hard rock, as
well as the purpose of such a monument at such a jTlace, will probably
always remain a mystery.
South of the Platte the Drift creeps to the surface on some of the hill-
sides of Lancaster, Saunders, Saline, Butler, Gage, Seward, Johnson,
Pawnee, and Jefferson Counties. In fact, there are few counties in the
eastern part of the State where the Drift is not occasionally exposed by
denudation. Four miles northwest of Nebraska City, on the farm of
Hon. J. F. Kinney, is a granitic bowlder as large as a small hoase, on
whose top smooth holes have been worn by the Indians in grinding ar
poauding corn. This bowlder m imbedded in a Loess deposit, through
which it extends from the Drift below. Here, as in most other regions,
the Drift varies a great deal in character. As already intimated, it has
here been so modified by subsequent lacustrine agencies as generally to
be capable of high caltivation. Eecently I have made a special exam-
ination of the modified Drift in Johnson County. Where the gronnd
was covered with pebbles, the spade showed that the soil beneath was
composed largely of Loess materials, mingled with Drift sand and clay«
and organic matter. Here it is often in layers, showing that it is gen-
uine modified Drift. This modified Drift soil, during the last season,
where it was well cultivated, yielded sixty bushels of corn to the acre-
It is only inferior, if inferior at all, to the Loess, which will be considered
in the next section. Where this Drift is the purest, it is composed of
bowlders, some of which are of large size, pebbles, gravel, sand, and a
small per cent, of alumina. In places the Drift contains considerable
lime, which was, no doubt, produced by the disintegration daring glacial
times of the Niobrara division of Cretaceous rocks. Sometimes fiug*
ments of these Cretaceous rocks are found in the Drift. Generally tl^
pebbles and bowlders are composed of the primary rocks, such as
quartz, quartzose, granite, greenstone, syenite, gneiss, porphyry, actino-
lite, &c. Occasionally the near presence of the Drift is indicated by
large bowlders sticking up through soil composed of very different mate-
rial. In such cases I have learned by experience to look for the modi-
fied Drift which is so valuable in the agriculture of this State. In tiie
few localities where all the finer matter has been removed l>y water
agency, numbers of the different forms of variegated agates, carnelians,
jaspers, sardonyx, onyx,opals, andpetrified wood, &c., are found. Agates
and petrified wood are specially abundant. The latter is found aloiost
in every exposure of the Drift. Some of the agates vie in beauty with
those obtained from the mt^st celebrated localities in the moautaiBS.
Judging from the remains of the matrix still attached to some of them,
they were originally formed in the primary rocks, from which they were
separated by the disintegration to which they were subjected by the
wear and tear of the elements in glacial times.
The scratchings on top of the rocks along the Platte and other rivers
where I have l^en able to examine them, indicate that the general
direction of the glaciers v^sls from 19^ to 27^ east of south. The only
exception to this direction that I have found was in Stoutfs stone-qaarry,
twelve miles southeast of Lincoln, on the Nebradca Bailroad, where th»
motion seems to have been 13.5^ degrees east of south.
«
AiGiiET.] , THE LOESS DEPOSITS. 245
A brief description of a remarkable section through the Drift on Oak-
Creek, Lancaster County, will not be out of place, A few miles from
Lincoln the terrace on this creek^ compo^d of Loess materials, ap-
proaches the creek very closely. In this well the Loess deposit was fifteen
ieet in thickness, then came two feet of Drift, then two feet of compact
peat, then clay and black soil, and then Drift again. The lower Drift
here probably represents the period of the first glacial advance. The
clay, black soil, and peat represent the middle period when the glaciers
had retreated and a new forest-bed covered the State. The Drift, imme-
diately on top of this, marks the second advance of the glaciers. The
Loess on top represents the final retreat of the glaciers, and that era of
depression of the surface of the State when the greater part of it con-
stitnted a great fresh- water lake into which the Missouri, the Platte, and
the EepubUcan Elvers poured their waters.
THE LOESS DEPOSITS.
The Loess deposits first received this name from Lyell, who observed it
closely along the Mississippi in various places. Hay den frequently calls it
the bluff formation, because of the peculiar configuration that it gives to
the uplands which border the flood-plains of theri vers. He also frequently
calls them marl-beds. This deposit, although not particularly rich in
organic remains, is in some respects one of the most remarkable in the
world. Its value for agricultural purposes is not exceeded anywhere.
It prevails over atjeast three-fourths of the surface of Nebraska. It
ranges in thickness from five to one hundred and fifty feet. Some sec-
tions of it in Dakota County measure over two hundred feet. At North
Platte, 300 miles west of Omaha and on the south side of the river,
some of the sections that I measured ranged in thickness from one hun-
dred and twenty-five to one hundred and fifty feet. From Crete, on the
Borllngton and Missouri River Bailroad, west to Kearney, on the Union
Pacific Kailroad, its thickness for 90 miles ranges from forty to ninety
feet. South of Kearney, and for a great distance west, along the Union
Pacific Bailroad as far as to the Eepublican, there is a great expanse of
territory covered by a great thickness of this deposit. I measured many
sections in wells over this region and seldom found it less than forty,
and often more than sixty feet in thickness. Along the Eepublican I
traced the formation almost to the western line of the State, its thick-
ness ranging from thirty to seventy feet. One section north of
Kearney, on Wood River, showed a thickness of 50 feet. The same
variation in thickness is found along the counties bordering on the Mis-
souri. One peculiarity of this deposit is that it is almost perfectly
homogeneous throughout, and of almost uniform color, however thick the
deposit, or far apart the specimens have been taken. I have compared
many specimens taken 300 miles apart, and from the top and bottom of
the deposits, and no difference could be detected by the eye or by chemicai
analysis.
Over 80 per cent, of this deposit is very finely comminuted silica.
When washed in water left standing, and the water poured off, and
the coarser materials have settled, the residuum, after evaporation to dry-
Bess, is almostentirely composed of fine siliceous powder. So fine, indeed,
are the particles of silica that its true character can alone be detected
by analysis or under a microscope. About 10 per cent, in composed of
the carbonates and phosphates of lime. These materials are so abundant
Id these deposits that they spontaneously crystallize, or form concretious,
from the size of a shot to that of a walnut; and these are often hollow
or contain some organic matter, as a fossil, around which the crystaliiza-
246
6E0L0QICAL SURVEY OP THE TERRITOKIES.
tion took place. Almost anywhere, when the soil is turned over by the
plow or in excavations, these concretions may be foond. Often, after a rain
lias washed newly-tbrown-op 8oil,*the ground seems to be literally cov-
ered with them. Old gopher hills and weather-beaten hillsides foroish
these concretions in unlimited quantities for the geologist and thecariosity
hunter. When first exposed, most of these concretions are soft enough
to be rubbed fine between the fingers, but they gradually harden by ex-
posure to the atmosphere. Tliis deposit also contains small amounts of
alkaline matter, iron, and alumina. For the purpose of showing the
homogeneous character and the chemical propertiesof the Loessdeposits,
I have made five new analyses of this soil. !No. 1 is from Douglas
County, near Omaha; No. 2 from the blnfi's near Kearney; No. Sis
from the Lower Loup ; No. 4 from Sutton, and No. 5 from the Bepub-
lican Valley, near Orleans, in Harlan County.
Insoluble (sUioeoas) matter
Ferric oxide
AlamLoa
Lime, carbonate
Lime, phosphate
Magnesia, carbonate
Potawa
Soda
Organic matter
Moisture
LofcSin analysis
No. I.
No. 8.
No. 3.
No. 4.
Xo.&
81.28
81.33
81.35
8L30
8I.»
3.86
3.87
3.83
3.85
3.86
.75
.■55
.74
.rj
.74
&07
&C6
B.03
6.05
&(•
3.56
3.59
3.58
3.57
a»
1.29
1.28
1.31
1.31
1.89
.27
.29
.35
.34
.33
.15
.16
.14
.16
.16
1.07
).G6
1.05
1.06
1.06
1.C9
1.C8
1.09
1.08
1.09
.59
.54
.53
.55
.47
100.00
100.00
loaoo
loaoo
icaoi
Since making the above analyses I have received from Dr. Hayden
his Final Beport on the Geology of Nebraska. This report, on page 12,
contains two analyses of the Loess deposit, from Hannibal, Missouri,
made by Dr. Litton. According to this analysis, from one hundred parts
there were —
Silica
Alumina and peroxide of iron
Lime
Magnesia
Carbonic aeid
Water
No. I.
76.98
77.08
11.54
I&IO
3.87
ass
1.68
1.63
Not. detenninecL
S.83
2l01
9.43
96.17
KOL S.
99.96
According to this analysis the Loess contains more clay in Missouri
than it does in Nebraska.
For the purpose of comparison, I here reproduce, from ITayden's re-
port, Bischoff 's analyses of the Lacustrine or Loess of the Rhine :
Silioioacid
Alumina
Peroxide of iron
Lime ,
Magnesia
Poiaah
Soda
Carbonate of lime
Carbonate of magnesia
Leas byignltien
No. of analysis.
1.
58.97
9.97
4.25
0.02
0.04
0.11
a 81
90.16
4 21
1.37
79.53
13.45)
4.8t>
0.03
0.r6
1.05)
1.145
7&61
15l26
0.09
3.31
L89
62.43
7.51
9l14
a 21
1.75
11.63
&31
61.04
9l75
iL67
asr
▲uiBHR.] THE LOESS DEPOSITS. 247
It will be seen from the above analyses of Biscboff tbat Nos. 3 and 5,
in tbe quantity of silica and otber elements tbat are present, come very
near tbe Loess of Nebraska. Tbe principal difference is tbe larger quan-
tity of alumina present in tbe samples analyzed by Biscboff. Gbemi-
(sally tbe deposits of tbe Bbine Valley, as Hayden remarks, are not
easentially different from tbose of tbe Loess soils along tbe Missouri.
As would be expected, from tbe elements wbicb cbemical analysis
shows to be present in tbese deposits, it forms one of tbe best soils in
the world. In fact, it can never be exbausted until every hill and valley
of wbicb it is composed entirely worn away. Its drainage, wbicb is tbe
best possible, is owing to tbe remarkably finely-comminuted silica of
wbicb tbe bulk of tbe deposit consists. Where the ground is cultivated
the most copious rains soon percolate through tbe soil, wbicb, in its
lowest depths, retains it like a huge sponge. Even the unbroken prairie
absorbs much of the heavy rains that fall. When droughts come the
moisture comes up from below by capillary attraction. And when it is
considered that tbe depth to the solid rock ranges generally from five
to two hundred feet, it is seen bow readily the needs of vegetation are
sapplied in the driest seasons. This is the main reason why over all the
region where tbese deposits prevail tbe natural vegetation and the well-
cultivated crops are rarely dried out or drowned out I have frequently
observed a few showers to fall in April, and then no more rain until
June, when, as will be considered farther on, there is generally a rainy
season of from two to four weeks' continuance. After these June rains
little more would fall till autumn; and yet, if there was deep and
thorough cultivation, tbe crops of corn, cereals, and grass would be
most abundant. This condition represents the dry seasons. On the
otber hand, the extremely wet seasons only damage tbe crops over the
low bottoms, subject to overflow. Owing to the siliceous nature of the
soils they never bake when plowed in a wet condition, and a day after
heavy rains the plow can again be successfully and safely used.
Tbe physical properties of the Lacustrine deposits are also remark-
able. In tbe interior, away from the Missouri, hundreds of miles of
tbese Lacustrine deposits are almost level or gently rolling. Not unfre-
quently a region will be reached where, for a few miles, tbe country is
bluffy or hilly, and then as much almost entirely level, with intermedi-
ate forms. The bluffs that border the flood-plains of the Missouri, the
Lower Platte, and some otber streams are sometimes exceedingly pre-
cipitous, and sometimes gently rounded off. They often assume fantas-
tic forms, as if carved by some curious generations of the past. But
now they retain their forms so unchanged from year to year, affected
neither by rain nor frost, that they must have been molded into their
present outlines under circumstances of climate and level very differ-
ent from tbat which now prevails.
For all purposes of architecture this soil, even for tbe most massive
structures, is perfectly secure. I have never known a foundation of a
large brick or stone building, if commenced below the winter frost-line,
to give way. Even when the first layers of brick and stone are laid on
top of the ground tiiero is seldom such unevenness of settling as
to produce fractures in the walls. On no other deposits, except
the solid rocks, are there such excellent roads. From twelve to
twenty-four hours after the heaviest rains the roads are perfectly
dry, and often appear, after being traveled a few days, like a vast floor
formed from cement, and by tbe highest art of man. The drawback to
this picture is that sometimes during a drought the air along the high ,
ways on windy days is filled with dust. And yet the soil is very easily.
248 GEOLOGICAL SURVEY OF THE TERRITOBIES.
worked, yielding readily to the spade or the plow. Excavatiou is
markably easy, and no pick or mattock is tbongbt of for sach purposes.
It might be expected tbat sacb a soil readily yielded to atmospberic in-
fluences, but sucb is not tbe case. Wells in tbis deposit are frequently
walled up only to a point above the water-line^ and ou the remainder
the spade marks will be visible for years. Indeed, the traveler over
Nebraska will often be surprised to see spade-marks and carved-oat
names and dates years after they were first made, where ordinary soils
would soon have fallen away to a gentle slope. This peculiarity of the
soil bas often been a God-send to poor emigrants. Such often cut oot of
the hillsides a shelter for themselves and their stock. Many a time
when caught out on the roads in a storm, far away from the towns, kavo
I found shelter in a '^dug-out" with an emigrant's family, where, oozy
and warm, there was perfect comfort, with little expenditure of fuel oa
the coldest days. In summer such shelters are much cooler than frame
or brick bouses. I shall never forget one occasion in 1866, when be*
wildered by a blinding snow-storm I came to a ^^ dug-out," and alUiongh
all the chambers were carved out of the soil (Loess) they were perfectly
dry. The walls were bidden and ornamented with Harper's Weekly^
with the emanations of Nast's genius made to occupy the conspicuous
corners. My hostess, whose cultivated intellect and kindly nature
made even this abode a charming resort, was a graduate of an eastern
seminary. Her husband, after a failure in business in Kew York, came
here to commence life anew on a homestead by stock-raising. To get a
start with young stock no money could be spared for a house. Eight
years afterward I found the same family financially independent and
living in a beautiful brick mansion, hut I doubt whether they had any
more substantial happiness than when they were looking for better days
in the old temporary ^'dugout." Thousands who are still coming into
this land of promise are still doing the same thing. So firmly does the
material of this deposit stand that after excavations are made in it, un-
der-ground passages without number could be constructed without meet-
ing any obstacles and without requiring any protection from walls and
timber.
Cati9€ of theie peculiariHe$.
These peculiarities of the Loess deposits are chiefly owing to the fact
that the carbonate of lime has entered into slight chemical combination
with the finely comminuted silica. There is always more or less carbonic
acid in the atmosphere which is brought down by the rains, and this
dissolves the carbonate of lime, which then readily unites with silica, but
only to a slight extent, and not enough to destroy its porosity. Though
much of the silica is microscopically minute, it has largely preserved its
angular structure, and tbis of course aids the slight chemical union that
takes place between it and tbe carbonate of lime. Bad there been more
lime and iron in this deposit, and had it been subjected to greater and
longer pressure from superincumbent waters, instead of a slightly chemi-
cally compacted soil it would have resulted in a sandstone formation
incapable of cultivation. There is not enough clayey matter present to
prevent the water from percolating through it as perfectly as through
sand, though a great deal more slowly. This same peculiarity causes
ponds and stagnant water to be rare within the limits of this deposit
Where they do exist in slight depressions on the level plain, it is found
that an exceptionally large quantity of clayey matter has been accumu*
lated in the soil on the bottom. In Clay, Fillmore, York, and a few other
counties there are considerable numbers of ponds, covering from a few
acres to half a section of land, grown up around the border with reeds
jkv^psT.] FRUIT OK THE LOE88 DEPOSITS. 249
and coarse grasses and sedges, and where the water is deeper, with
arrow-leaves, poDd-lilies, and other water-plants. In every instance
where I had opportunity to examine them, there was a thin bed of clayey
matter mixed with organic materials, from a few inches to a foot or more
in thickness, lying on the bottom, and on top of the Loess deposit. This
clayey matter was probably deposited there before the waters finally
retired from the old lake-bed in which this soil originated. In the stiller
I>ortion3of the lake, or in eddies, about the time it commenced to become
dry land, when portions were already cut off from the main lake, except
io flood-time, in these isolated pools all the clay in solution would be
precipitated to the bottom, before the next annual rise of the waters.
This I propose as a provisional explanation of this phenomenon.
Fruit on the Loess deposits.
In these Loess deposits are found the explanation of the ease with
which nature produces the wild fruits in Nebraska. So dense are the
thickets of wild grapes and plums along some of the bottoms and bluffs
of the larger streams that it is difficult to penetrate them. Over twenty
varieties of wild plums have been observed, all of them having originated
either from Prunus amerieanOy P. ehiolcasa,^ or P. permiHo. Only two
species of grapes are clearly ontlined, namely, Vitis aestimlis and F.
cardifolia^ but these have such interminable variations that the botanist
becomes discouraged in attempting to draw the lines between them, and to
define the range and limit of the varieties. The same remark could
be made of the strawberries. Raspberries and blackberries abound in '
many parts of the State. The buffalo-berry {Shepheriia canadensis) is
common on many of the Missouri and Bepublican River bottoms.
Man3' other wild fruits abound, and grow with wonderful luxuriance
wheiever timber protects them and prairie-fires are repressed. A a
would be expected, these deposits are also a paradise for the cultivated
fruits of the temperate zones. They luxuriate in a soil like this, which
has i)erfect natural draiuage, and is composed of such materials. No
other region, except the valleys of the Nile and of the Bhine, can, in
these respects, compare with the Loess deposits of Nebraska. The Loess
of the Bhine supplies finrope with some of its finest wines and grapes.
The success that has already attended the cultivation of the grape, in
Southeastern Nebraska, at least, demonstrates that the State may
likewise become remarkable in this respect. For the cultivation of the
apple its superiority is demonstrated. Nebraska, although so young
in years, has taken the premium over all the other States in the porno-
logical fairs at Bichmond and Boston. Of course there are obstacles
here in the way of the pomologist as well as in other favored regions.
Bat what is claimed is, that the soil, as analysis and experience prove,
is eminently adapted to grape, and especially to apple*tree culture. The
chief obstacle is particularly met with in the interior of the State, and
results from the climate. In mid-summer occasional hot, dry winds
blow from the southwest. These winds, where the trunks of apple-trees
are exposed, blister and scald the bark on the south side, and frequently
kill the trees. It is found, however, that when young trees are caused
to throw out limbs near to the ground, they are completely protected,
or if that has not been done, a shingle tacked on that side of the tree pre-
vents all damage from that source. Many fruit-growers also claim that
Cottonwood and box-elder groves on the south side of orchards is all
that is necessary to protect them from these storms. I mention this
here to put any new settler, who may read this and who has not learned
the experience of fruit-growers in this State, on his guard.
250 GEOLOGICAL SURVEY OP THE TEBRITORIES.
Scenery of the Loess d^osits.
It has been remarked that ^'no sharp lines of demarkation separate the
kinds of scenery that produce the emotions of the grand and the bean-
tiful." This Is eminently true of some of the scenery produced by the
Loess formations. Occasionally an elevation is encountered from whose
summit there are such roagniflcent views of river, bottom, forest, and
winding bluffs as to produce all the emotions of the sublime. One such
elevation is Pilgrim Hill, in Dakota County, on the farm of Hon. J.
Warner. From this hill the Missouri bottom, with its marvelous, weird-
like river, can be seen for twenty miles. Dakota City and ISioux City,
the latter distant sixteen miles, are plainly visible. If it happens to be
Indian summer, the tints of the woods vie with the hazy splendor of the
sky to give to the far outstxetched landscape more than an oriental splen-
dor. I have looked with amazement at some of the wonderful canons
of the Eocky Mountains, but nothing there more completely filled me
and satisfied the craving for the grand in nature than did this view from
Pilgrim Hill. Another view equally majestic is on the Missouri, back of
lona, in Dixon County. My attention was directed to it by John Hill,
esq., who took me to the West point for observiug the river, which can
here be seen for a great distance. The alternations of lofty bluff and bo^
torn, woodland and prairie, give a picture worthy the pencil of the most
gifted artist, and of all who love the grand and picturesque in nature.
It is true that suchscences are rare, but then there are many landscai)e3
which, if not grand, are still of wonderful beauty. This is the case along
mostof the bluffs of the principal rivers. In Northern Nebraska these
bluffs often reach two hundred or more feet in height, and this perhaps
gives this portion ot the State the most varied scenery. At some points
these bluffs are rounded off and melt beyond into a gently-rolling plain.
But they constantly vary, and following them you come now into a beau-
ful cove, now to a curious headland, then to terraces, and, however far
you travel, you in vain look for a picture like the one just passed. Nu-
merous rounded tips, with strangely precipitous sides, are seen in every
hour's travel, and these, as they form bold curves, rampart-like, stretch
away into the distance and form images of the most impressive beauty.
Indeed the bluffs of the Loess deposits are unique, and^ Buskin cannot
exhaust the subject of the beautiful until he sees and studies the hills of
Nebraska.
Origin of the Icieuatrine deposits.
The geological discoveries .of the last decade, and especially those of
Dr. Hayden, indicate that there have been no breaks in geological his-
tory, if this view is correct, then the Glacial age was not suddenly
inaugurated, as was once held. At least, during the latter portion of tbe
Pliocene age, the temperature was steadily falling from year to year.
It may have been so slow as to be only perceptible in the course of cen-
turies. Finally, however, glaciers formed in tbe polar regions. Grad-
ually, by the continually-falling temperature, these glaciers crept
southward from the polar regions, until, in the course of ages, tbey
covered the whole land down to perhaps the thirty-fifth degree of north
latitude. It was during this period tbat, x)eihaps, most of tbe glacial
scratches and other markings of these times, so familiar to the geologist,
were made all over the north temperate zone, from the thirty-fifth de-
gree towards the pole. After the glaciers had done their work, during
a period whose length is undetermined, a new change of level and o(
climate was inaugurated, and the ice-fields began to wane and gradually
AUGHTT.) ORIGIN OF THE LACUSTRINE DEPOSITS. 251
to disappear. This eatlre region becaine so depressed tbat the greater
part was submerged. How long this subniergence lasted is an unsolved
problem. As the land in the course of ages emerged again from the
waters, under the influence of a milder climate, it gradually became
covered with a vast forest. The bed of this old forest is often struck in
digging wells in many parts of the West. It is often found in the gla-
cial Drift, and separates it into two portions. It is composed of black
soil, and where I have measured it, its thickuess ranged from six inches
to three feet. It often contains partially decayed and partially or en-
tirely petrified wood. Over this old and now buried forest-bed the ele-
phant {Elephas ainerieanus) and mastodon {Mastodon amerieanm) roamed
in company with the i-eindeer and musk-ox. A back molar of the left side
of the lower jaw of an elephant, obtained from this old bed in Saline
County; which is in the university cabinet, measures seventeen inches from
frolit to rear. But the slow upward movement of the land, accompanied
by a gradually-falling temperature, inaugurated a second advance of the
glaciers, which '^ wiped out" the forests that covered the land. This
period was followed by a still greater subsidence of the land toward the
north, when the^ glaciers began to disappear the second time. Accord*
ing to Professor Newberry, who has profoundly studied this question, all
that region north of the Ohio, and westward beyond the Missouri, which
is now less than eleven hundred feet above the level of Lake Erie, was
covered with water. The depression was greatest toward the north, so
that in the east the Allegbanies, and their dependent foothills, and a
wide area of low country toward the south and west, formed a shore-
line to the interior sea of the period. This sea was often covered with
floating icebergs, which, melting, dropped their imbedded sand, gravel,
and bowlders to the bottom. The old controversy concerning the method
by which the glacial Drift was formed had on both sides some elements
of truth. It was formed exclusively by neither glaciers nor icebergs,
but by both operating at different times in their own peculiar way.
From this submergence the land slowly arose, and when the Missouri,
the Platte, and the Republican Eivers in their upper courses resumed
their worK the Lacustrine age commenced. There is, of course, no
exact line where the one ends and the other begins, but it is safe to say
that the later centuries of this great subsidence witnessed the deposi-
tion of the Loess deposits. When it commenced, the greater part of Iowa
had become dry land. What was left of this great sea was the western
portion of Iowa, a large portion of Nebraska, and the various lakes
along the Missouri^ in the States through which it flows on its way to
the Gulf. The Missouri, and sometimes the Platte, haVe been among tbe
mmldiest streams in the world. If we go up the Missouri to its source,
and carefully examine the character of the deposits through which it
passes, we cannot be surprised at its character. These deposits being of
Tertiary and Cretaceous ages, are exceedingly friable and easy of disin-
tegration. The Tertiary, and especially the Pliocene Tertiary, is largely
siliceous, and the Cretaceous is both siliceous and calcareous. In fact,
in many places the Missouri and its tributaries flow directly over and
through tbe chalk-beds of the Cretaceous deposits. From these beds
the Lacustrine deposits no doubt received their large per cent, of the
phosphates and carbonates of lime. Flowing through such deposits
for more than a thousand miles, the Missouri and its tributaries have
been gathering for vast ages that peculiar mud which filled up their
ancient lakes, and which distinguishes them even yet from most other
streams. Being anciently, as now, very rapid streams, as soon as they
emptied themselves into these great lakes, and their waters became
252 GEOLOGICAL SURVEY OF THE TEERITOBIES.
quiet, the sediment held suspended was dropped to the bottom. While
this process was going on in the earlier portion of this age, the last of the
glaciers had probably not retreated farther than the headwaters of the
Platte, the Missoari, and the Yellowstone. The tremendous force of
these mighty rivers was, for a while at least, aided by the erosive action
of ice, and therefore must have been vastly more rapid at times than
anything of the kind with which we are now acquainted. The follow-
ing analysis of Missouri River sediment taken at high stage will show,
by comparison with the analyses of the Loess deposits, what a remark-
able resemblance there is even 3'et between the two substances.
In one hundred parts of Missouri River sediment, there are of-—
Insoluble (siliceous) matter 82.01
Ferric oxide 3.10
Alumina 1.70
Lime, carbonate 6.50
Lime, phosphate 3.00
Magnesia, carbonate 3 .10
Potassa , 50
Soda 22
Organic matter IJiO
Loss in analysis 67
100.00
Two other analyses which I made, the one from sediment at high
water and the other at low water, differ somewhat from this, but in es-
sential particulars are the same. This identity of chemical combina-
tions also points to the remarkable sameness of conditions that have
existed for long periods in the Upper Missouri and Yellowstone regions.
After these great lakes were filled with sediment (Missouri mud), they
existed for a longer or shorter time as marshes or bogs. Isolated iK>r-
tions would first become dry land, and as soon as they appeared alK>ve
the water they were, no doubt, covered with vegetation, which, decay-
ing from year to year, and uniting under water or at the water's ed^
with the deposits at the bottom, formed that black soil so characteristic
of Nebraska prairies. For it is well known that when vegetable matter
decays in water or a wet situation its carbon is retained. In dry aitua-
tious it passes into the atmosphere as carbonic-acid gas. After the fir»(
low islands appeared in this old lake, they gradually increased from year
to year in size and numbers. The ponds and sloughs, some of which
could almost be called lakelets, still in existence, are probably the last
remains of these great lakes. These ponds, where they do not dry up
in midsummer, swarm with a few species of fresh-water shells, espe*
cially of the JAmnass^ Fkyaws^ and Plauarbij which to me is strong
proof of this theory of tbeir origin. The rising of the land oontinaingy
the rivers began to cut new channels through the middle of the old lake-
beds. This drained the marshes and formed the bottom-lands, as the
river-beds of that perioil covered the whole of the present flood-plains
from bluff to bluff. It was then that the bluffs which now bound these flood-
plains received those touches from the hand of nature that gave them
their peculiar steep and rounded appearance. Newer and more plastic,
because less compactly bound and cemented together, the rains and
floods easily molded them into those peculiar outlines which they have
since preserved* The Missouri, during the closing centuries of the I^
custrine age, must have been from five to thirty miles in breadth, forming
a stream which for size and majesty rivaled the Amazon. The Platte,
AUGBfiT.] LEKGTH OP THE LOESS AGE. 263
the ^Niobrara, and the Bepnbliean covered their respective flood-plains in
the same way. In the smaller streams of the State, those that origin-
ated within or near the Lacustrine deposits, such as the Elkhorn, Loap,
IBawj Bine, and the Nemahas, we see the same general form of flood-
plain as on the larger rivers, and no doubt their entire bottoms were
alao covered with water daring this period. Hayden, in his first reports,
has already expressed the same opinion as to the original size of these
rivers. Only a few geologists will dissent from this view. The gradu-
ally melting glaciers, which had been accumulating for so many ages at
the sources of these great rivers, the vast floods of water caused by the
Beoesaarily moist climate and heavy rains, the present forms and mate-
rials of the river-bottoms, are some of the causes which in my opinion
would operate to produce such vast volumes of water.
The changes of level were not all upward during this age. The ter-
races along the Missouri, Platte, and Bepnbliean indicate that there
were long periods when this portion of the continent was stationary.
Ouce, nt least, the movement was downward. Along the blufiTs in the
Kepublican Valley, at a depth varying from ten to thirty feet from the
top, there is a line or streak of the Loess mingled with organic matter.
It is, in fact, an old bed, where vegetation must have flourished for a long
period. It can be traced from Orleans upward in places for seventy-
five miles. It indicates that after this bed had, as dry land, sustained
a ^owth of vegetation, an oscillation of level depressed it sufficiently
to receive a great accumulation of Loess materials on top of it. I hare
found traoes of this movement in many other portions of the State.
Length of the Loess age.
The bases for speculation concerning the length of the Loess age are
of course uncertain, yet an approximate estimate may perhaps be made
by comparison with the present deposits of the Missouri. The great
lakes of the Loess age extended, with few interruptions, almost to the
Gulf, and some of them covered an area of at least 75,000 square miles.
Now, were all the sediment which is at present brought down the Mis-
souri spread over such a vast area, the thickness of the deposit would
be less than one-sixteenth of an inch. Probably the yearly accumula-
tions of sediment during the Loess age amounted to that much, owing to
the then greater volume of the Missouri and the aids to erosion from
the greater prevalence of ice near its sources. In many places along
the Missouri there are small lakes, formed from the old river-bed, where
there has been a cutoff. Even where these little lakes receive the
overflow of the river each year, it often requires at least a century to fill
them up, even when aided by the sands which the winds waft into them.
I have attempted to measure the sediment left by the river in these
lakes, which are seldom half a mile in breadth, and it rarely amounted
to half an inch in a season. The winds are a much more efficient agent
for filling up small, narrow lakes, but in Loess times, where there were
such immense bodies of fresh water, their effects could only have been
appreciable along the sandy shore-lines. The highest bluffs represent
the original level of the Loess deposits before the tremendous denuding
agencies which removed so much of their materials had done their
work. Now, in places these sediments are even yet 200 or more feet in
thickness, so that it would be safe to estimate the average thickness of
the original deposit at 100 feet. A yearly increase of one-sixteenth of
an inch in thickness, would at this rate have required 19,200 years to
form these deposits. This I consider a low estimate for the length of
the Loess age.
254 GEOLOGICAL SUB VET OF THE TEBBITOBIES.
lAfe of the Loess age.
At the «Io8e of this article will be found a list of ike land and fresh-
water shells that I have found and identified in the Loess deposits. It
will be seen that the list of land shells is qnite large. These, no doabt^
were brought into this old lake during flood-time. I have occasionally
found large numbers of these shells where drift-wood had evidentlj
lodged and decayed. The fresh-water and land shells are mainly socb
as are still to be found in the same region, the exceptions bein^ the
prevalence of a large number of southern forms at one horizon of these
deposits. As will be seen, the species belong to quite a large number of
genera.
Occasionally I have found the teeth and a stray bone of fish, bat
have not been able to identify any species. The remains of rabbits,
gophers, otters, beavers, squirrels, deer, elk, and buffalo, are frequently
found. Through the entire extent of these deposits are many remains
of mastodons and elephants, whose last vigorous life, as Newberry re-
marks, expired in high northern latitudes. Lancaster County is specially
rich in these proboscidian remains. They are frequently found in this
deposit in digging wells. In Lincoln they have been found in at least
twenty wells that have been dug in and around the city. This town is
near what appears to have been the western shore-line of the Misnonri
lake of the period. Between it and the Blue River, at Crete, there is a
high divide covered by Drift materials. These huge animals no doubt
often here came down to the shore to drink, and playing in the water
became mired in the mud. One tusk found in a well on P street, east of
Twelfth, must have been at least eleven feet long when entire. It was
so far decayed that it fell to pieces on exposure.
For years' I have been closely watching for human remains in the
Loess deposits. Five years ago, three miles east of Sioux City, lowa^
in a railroad-cut I found a small arrow-head in these deposits. I was
looking for mollusks, and was digging after them with a large knife
when I struck something hard, and, laying it bare, to my great surprise
and joy found it to be an arrowhead. So far as I knew, this was the
first mark that had yet been discovered of the presence of man during
this age. From that time onward I have seized every opportunity for
exploring these deposits for human remains. The same year I ionnd
some flint chips in the bluffs back of Jackson, in Dakota County, but it
was not absolutely clear that these were of human origin. My next find
was about two and a half miles southeast of Omaha, in a railroad-cut,
where I found a lar^e coarse arrow or spear head. This last was found
two years ago. It was found twenty feet below the top of the Loess,
and at least six inches from the edge of the cut, so that it could not have
slid into that place. The first found was filteen feet below the top of
the deposit. Figure No. I is the arrowhead found east of Sioux City,
and No. 2 found southeast of Omaha. It appears, then, that some old
races lived around the shores of this ancient lake and paddled their
canoes over its waters, and accidentally dropiied their arrows in its
waters or let them fly at .a passing water-fowl. It is possible also that
these arrows came into this old lake by drift-wood. I once found au
arrow sticking in a log that came down the Missouri, and if it had con-
tinued on to the Gulf it might have been unearthed in the far-off future,
when that portion of the continen't at the mouth of the Mississippi had
become dry land. Thirteen inches above the point where the last-named
arrow was found, and within three inches of being on a line with it^ in
undisturbed Loesis, there was a lumbar vertebra of an elephant {Elqfkoi
ATCBKT.l UPE OP THE LOE88 AGE. 255
americaniu). UDfortoaately this vertebra itartially fell to pieces on ex-
posDre. It appears clear from tbis conjunction of a fanmaD relic and
prolNWcidiaii remains that man here as weil as in Europe was the cotetn-
poniiy of the elephaot in at least a portion of the Miasoari Valley.
I^^l
Arrows found in tite Loeag.
No. 1. Foand thre« miles east of Sioaz City, Iowa, fifteen feet below
the sarface.
No. 2. Found two miles and a half soatheast of Omaha, Nebr., twenty
feet below the surface and beueath a vertebra of au elephant.
The trlimate probably varied coDsiderably daring the progress of this
age. What iuclioes me to that view is the fact that about the middle
horizon au unusually large number of southern species of moUnsks are
found. This indeed is uot conclusive, as this region ia at this time re-
markable for tbe presence Of southern forms of insects and fresh-water
mollasks.* Yet it appears to me that the unusual number of southern
forms at this horizon of tbe Loess must indicate some modiflcatiou of
cUmate at that period. It may have been only oa the eastern shore of
this great lake, and caused by the even temperature which so large a
body of freah water produces on tbe side toward which the prevailing
winds from tbe lake blow. We have sucb a phenomenon at the present
day on the east shore of Lake Michigan. The Mississippi Valley is by its
contour emiueotly favorable to the emigration northward of sontfaem
Biiecies.
These Loess deposits, which have done so much to enrich Nebraska,
have received profound attentiou and study from some of the ablest
geologists. But in more than one-half of the counties of the State they
have not yet been investigated. Much tobediscoveredmnst yet remain
in them. Though myself long engaged in their investigation, I nirely
examine a new section in a well, ravine, or railroad-cut without finding
something new.
* Hftjdeo'i Beport for 1870, p. K7.
256 GEOLOGICAL 6tTRT£Y OF THE TERBITOBIES.
ALLtrVltJM.
I^ext to the Loeiss deposits, in an economical point of view, the Alia-
vinm formations are the most important. The valleys and flood-plains
of the rivers and smaller streams, where these deposits are fonod, are a
prominent feature of the surface geology of the State. All the rivers of
the interior, snch as the Platte^ the Republican, the Niobrara, the Bow, the
Elkhoru, the Blues, the Nemahas, and their tributaries, have broad
bottoms, in the center or on one side of which the streams have their
beds. The width of these bottoms seems to be dependent on the char-
acter of the underlying rock-formation. Where this is soft or yielding
the bottoms are broad, but where it is hard and compact they contract.
This is, no doubt,' one reason why the bottoms on the middle or upper
courses of some of the rivers are wider than farther down.* These broad
bottoms, as we have already seen, represent the ancient river-beds
toward the close of the Lacustrine age. It required many ages to drain
this mighty ancient lake-bed ; and when the present rivers were first
outlined, the greater part of it was yet a vast swamp or bog. But,
gradually, as the continent' rose to a higher level, the rivers cut deeper
and deeper, filling the whole flood-plain from bluff to bluff. Not until
the drainage of this region was completed and the continent had reached
nearly its present level was the volume of water so much diminished
that the rivers contracted their currents and cut new beds somewhere
through the present bottoms. The terraces, which are so numerous
along many of the river- bottoms, indicate the slowness with which the
land assumed its present form. They mark those stages of elevation
when the land was stationary. The upper terraces were' dry bottom
when all the rest of the valley was yet a river-bed. It is probable
that some of these bottoms were excavated during sub-glacial times,
and afterward were filled up with dSMs when the continent had reached
its lowest level. The great depth of sand and mud at the bottom of the
Missouri, being from forty to one hundred feet below low water alon^ the
Nebraska line before solid rock is reached, indicates an elevation of this
region, when this was accomplished, far greater than it reached at any
period during Loess times. When this great lake commenced to be
drained the waters naturally took the direction and place of least
resistance, which was the original bed of the river. If the Bocky
Mountain system continues to rise, as it is believed to be doing, at the
rate of a few feet to the century, although degradation may be equal to
elevation, a time must come in the distant future when the Missouri will
again roll over solid rock at its bottom.
As typical of the river-bottoms, let us look at the formation of the
Platte Valley. The general direction of this great highway from the
mountains to the Missouri is from west to eaBt. This valley is ftom
three to fifteen miles wide in Nebraska, and over fire hundred miles long.
All the materials that once filled up this trough, from the top of
the highest hills on each side, have been, since the present rivers were
outlined toward the close of the Lacustrine age, transported by the
agency of water to the Missouri and the Gulf.t Here, then, are several
thousand miles in area of surface entirely removed by denudation. Now
the Platte comprises only a fraction of the river-bottoms of Nebraska.
The Eepublican alone for two hundred mites has a bottom ranging
from three to eight miles in breadth. The combined length of the main
bottoms of the Blues, Elkhorns, and the Loups would be over a thou-
* See on this subject Hayden*s Beport ibr 1670.
t Hayden's Beport for 1870. •
AuoBBT.l ALLUVIUM OF NEBRASKA. 257
sand miles, and their breadth ranges from one to ten miles. The
Maba« and the Bows, and portions of the Niobrara, also add a great
deal to the area of bottomlands. All these rivers faave numerous trib-
utaries, which have valleys in size proportionate to the main rivers,
and these more than double the areas of bottom-land. The Missouri
has, also, in some counties, like Dakota and Burt, contributed large
areas of bottomland to the soil of the State. These Missouri bottoms
in Nebraska are exceptionally high, so that few of them have been over-
flowed since the settlement of the country. The one element of uncer-
tainty about them is, wheu located near the river the danger of being
gradually washed away by the undermining action of the water. Some-
times during flood-time, when the current sweeps the bank, it is so insid-
iously undermined that, for several rods in length and many feet in
breadth, it tumbles into the river. This cutting of the rivev is greatest
when it commences to fall. Where the bank is removed on one side it
generally is built up on the other. The old town of Omadi, in Dakota
County, is an instance of this kind. So rapidly did the river cut into
the bank tnat many of the houses could not be removed, and fell victims
to the flood. The river cut far enough to the west of the old site to leave
it and its own bed, after being blown full of sand, to be grown up into a
forest of Cottonwood.
When now we bring into our estimate all the river-bottoms of Ne-
braska, and the tributaries of these rivers, and reflect that all these
valleys were formed in the same way, within comparatively modern
geological times, the forces which water-agencies brought into play
almost appall the mind by their very immensity. So well are these
bottom-lands distributed that the emigrants can, in most of the
counties of the State, choose between them and the uplands for their
future home. In some of the few counties, like Fillmore, where
bottom-lands are far apart, there are many small, modern, dried-up
lake-beds, whose soil is closely allied to that of the valleys. Not
unfrequently is the choice made of portions of each, on the sup-
position that the bottom-lands are best adapted for the growth of
large crops of grasses. But all the years of experience in cultivating
uplands and bottoms in Nebraska leave the question of the superiority
of the one over the other undecided. Both have their advocates. The
seasons as well as the location have much to do with the question.
Some bottom-lands are high and dry, while others are lower and contain
so much alumina that in wet seasons they are difficult to work. On such
lands, too, a wet spring interferes somewhat with early planting and
sowing. All the uplands, too, which have a Loess origin, seem to pro-
duce cultivated grass as luxuriantly as the richest bottoms, especially
where there is deep cultivation on old breaking. Again, most of the
bottom-lands are so mingled with Loess materials, and their drainage is
so good that the cereal grains and fruits are as productive on them as
on the high lands. The bottom-lands are, however, the richest in or-
ganic matter. The following analyses of these soils will give a better idea
of their chemical and physic^ character. The samples were taken from
what are believed to be average soils. The first is from the Elkhorn,
the second from the Platte, the third from the Bepublican, and the
fourth from the Blue Biver. The fifth is irom an exceptionally wet and
sticky soil, about two miles southeast of Dakota Cttty.
17 H
258
OEOLOOICAL SURVEY OF THE TERRITOBIES.
Ko.1.
No. 2.
No. 3.
No. 4.
■
So. 5.
TnRolablp ^Ailicpoafl) matter .,......,t.r-,,,T---.T.-,r
63.07
3.85
8.41
7.08
.»)
1.41
.5«»
.49
.?}»
14.(0
50
63. 7»)
2.25
7.76
7.99,
.83
I.4.S
.54
.52
.70
li.45
.79
63.01
2.40
8.36
8.01
.99
1.39
.61
..M
.71
laui
.97
100.00
•
62 99
2.47
8. (.8
7. 8.)
94
1.40
.67
.r8
.*;9
13.27
.96
l>1.^3
pBrrlo oxide ............ .......................
5L><2
Alumina ,m
111 52
I^lmf-. curhonntfl m...r,-r,-.-,r -r,,T-,-,
7.19
tiime. nhoBnhate .............................................
.48
Mmnieain. cOifboiiHtfl .........................................
l.itd
Potash ...u .....rr
.6)
Soda
.w
SQlDhuric acid -
.(»
OrarflDic matter
13.4»J
liOMin aiiftlysbi
.Itt
(
ICO. 00
100.00
ICO. 00
ICKi.00
It is well kDowD tlmt many soils vary a great deal in chemical prop-
erties that are taken only a few leet apart, and therefore analynes often
fail to give a con-ect ideii of their true character. Bat from the above
analyses, taken from widely distant localities, it is at least evident that
ohetnically, allavium diiiers from the Loess deposits, principally in having
more organic matter and alumina, and less silica. The depth of the
alluvium varies greatly. Occasionally sand and drift materials predomi-
nate in the river-bottoms, especially in the subsoil ; sometimes the alla-
vium is of unknown depth, atid again in a few feet the drift pebbles
and sand of the subsoil are struck. This is especially the case in soma
of the western valleys which were worn down to the dritt, and were
not again subsequently filled up, though sach cases are not often
met with. There must have been a f>eriod of longer or shorter
duration, when the bottoms were in the condition of swamx>s and
bogs; and during this period the greater part of that organic mat-
ter, which is a distinguishing feature of these lands, accumulated in the
sorfacesoil. It would be easy to select isolated spot«i, where the soil
has forty per cent, of organic matter ; where, in fact, it is composed of
semi-peat. When we reSect that this black soil is often twenty feet
thick, it is apparent that the period of its formation mast have been
exceedingly long. There are still some few localities where that forma-
tive condition has been perpetaated to the present time — as, for ex-
ample, the bogs that are yet met with at the headwaters of the Elk-
horn and the Logan, along the Elk Creek, on the Dakota bottom, and on
Stinking Eiver, one of the tribatarles of the Republican. In fact^ along
these tributaries all the intermediate stages from perfectly dry bot-
tom to a bog can yet be found. But, so much has the volume of water
been lessened in all the rivers of Nebraska through the inflnence of geo*
logical canses, thai tbere are few places where now, even in flood-time,
they overflow their banks. A curious phenomenon, illnstratingthroag'h
what changes of level and other conditions these river-bottoms have
passed, before reaching their present form, is the occurrence at vanonsi
depths, of from ten to fifty feet, of great masses of timber in a semi-
decayed condition. One snch de{>osit on the Blue River iHiitom, near
the mouth of Turkey Oi«ek, successfully interrupted the digging of a
well. So many thicknesses of logs o<M;nrred that it was found l^st to
abandon the work already done for a new place. I have frequently ob-
served trees, with trunks twenty to sixty feet long, sticking out from un-
der the banks of the Missouri, where the soil had been freshly removed.
It is possible that this timber accnmnlate<l in these places during the
period when the rivers yet covered their entire bottoms, and when num-
berless trees must have been carrie<l down during flood-time, and either
stranded on the ancient sand-bars and mud-banks, or sunk to rise uo
AucHET.l NEBRASKA — THE SAND-HILLS. 259
more in the deeper pools and eddies which were rapidly filled op. The
species, so far as I have yet been able to determiQe, from an examina-
tion of the half-decayed wood, are the same as yet grow in this region.
They are principally cottonwood, elm, cedar, maple, and walnat.
THE SANDHILLS.
The sand-hills are an often-mentioned portion of Nebraska. They
are found in certain sections of the western portion of the State. South
of the Platte Valley they ran parallel with the river, and are from one-
half to six miles in breadth. A few are also found on the tributaries of
the Bepnblican. Occasionally slightly sandy districts are found as far
east as the Elkhom, but they rarely approach even a small hill in mag-
nitude. North of the Platte, from about the month of the Calamus on to
the Niobrara, they cover much larger areas. They are also found over a
limited area north of the Niobrara. Hayden (Heport for 1870, p. 108)
estimates the area of the sand-bills at about 20,000 square miles. From
exploring the same region, I should not estimate them as so extensive,
unless the fact be kept in mind that they are not continuous over the
whole region. They are indeed found all the way for 100 miles west
from the mouth of Bapid Biver, but in many places from eight to twenty
miles south of the Niobrai*a there are spots where the soil seemed to be
a mixture of Drift and Loess, and of high fertility, as was indicated by
tbe character and rankness of the vegetation. Sometimes these hills
are comparatively barren, and then again they are fertile enough to
sustain a scant covering of nutritious grasses; so that this region is by
no n^eans the utterly barren waste that it is sometimes represented to
be. It has been a favorite range for buffalo, and still is for antelope
and deer ; and, judging from their condition, the conclusion would be
natural that this region could be used for stock-raising. A great deal
of the vegetation is peculiar to sandy districts. Some of the hills seem
to have their loose sands held together by the Toca angmtifoliaj which
sends its roots down to a great depth. It probably marks a certain
stage in their history. After this plant has compacted and given to the
sands organic matter, the grasses come in and partially clothe the hills.
The materials of these sand-hills are almost entirely sand, pebbles, and
gravel, of varying degrees of fineness. The sand always predominates.
Occasionally it is more or less modified by the presence of other mate-
rials, such as lime, potanh, soda, alumina, and organic matter. These
hills are in some places stationary, and so covered by vegetation that
their true character is not suspected until closely examined. In other
places again, especially in portions of the Loup and tlie Niobrara region,
they are so loosely compacted that the wind is ever changing their form,
and turning them into all kinds of fantastic shapes. The most common
appearance is that of a plain, undulating, or hilly region, covered with
conical hills of drifting sands. The smaller elevations frequently show
striking resemblance to craters. One such curious hill I found south of
the Calamus, where the crater-like basin seemed to be compacted at
once, and grown over with a species of wire-grass.
Some eminent geologists have sought to account for these hills by
the theory that the winds in the coarse of ages have blown the sand
from the bars on the rivers until their accumulation caused these pecu-
liar elevation^ There are many difiBculties in the way of this theory.
East of Columbus no sand-hills are found, and it is hard to conceive
how they should come to be limited to the western portion of the State
if t^ey were formed in this way. In some places at least the hills are
2S0 GEOLOGICAL 8UBTEY OF THE TEBRITOBIES.
partly composed of large iiebbles and stones that could not bave been
moved by the winds. This is especially the case in some of these hills
south and east of Kenesa.w, in Adams County. I suggest, as a pro-
visional explanation, the probability that south of the Platte the lines of
sand-hills show the track of a current in the old lake that produced the
Loess deposits. It is well known that fine sediment is deposited in still
water, but coarse materials, such as sand and pebbles, in the borders
and in tracks of currents. As the whole country rises toward the
west, the water here may have been very rapid, and the land in pro-
cess of drying up when it was yet deep at lower levels. Both cansesi
the currents and the winds, may have co-operated to produce these de-
posits. I am also satisfied that in some localities the sandhills are
nothing more than modified Loess deposits. They are Loess deposita,
with all the alumina, organic matter, and finest sands washed oat of
them. This at least seems to be the origin of some of the sand-hills
on the Lower Loup, where they occupy a lower level than the Loess de-
posits. These two deposits so often shade into each other in the neigh-
borhood of the sandhills, rendering it impossible to tell where the one
begins and the other ends, that the theory of their common origin
best explains the phenomena of these formations. After the western
portion of the Loess deposits first became dry land, water-agencies were
yet so powerful, especially in flood-times, that much of it most have
been remodified, and the coarser materials left to form sand-hills. On
the other hand, the sand-hills on the Upper Loup and the Niobrara
probably derive<lthe bulk of their materials directly from Pliocene Ter-
tiary deposits, which were mainly loosely-compacted sands. This old
Pliocene lake was probably peri>etnated here down through Loess times
to the borders of our own era. Even yet lakelets are nnmeroos over
portions of this region, some of which are alkaline and others fresh-
water. The latter can easily be distinguished from the former at sight, by
the thick vegetation growing around their margins, of which the former
have very little, and sometimes not a trace. It is at least evident that
these freshwater lakes have had some common origin. Their faona
would prove it. The same species of fish and fresh-water mollnsks are
found in most of the large ones, even where there is no perci'ptible
present outlet.
Although opposed to the views of eminent scientists, I have no doabt
that many of these hills are capable of cultivation and some day will be
cultivated. Not, indeed, until the rich lands that border them are im-
proved. But when better lands become scarce and costly, advances
will gradually be made on the sand-hills. Already it has been proved
that they produce sweet-potatoes and other root-crops equal at least to
the New Jersey sands. The rich marl-beds in their vicinity will supply
an inexhaustible source for fertilizing them.
Much as has been done by Hayden and others in exploring these sand-
hills, still much more remains for the geologist before all the causes
that produ<^ them are thoroughly understood.
ALKALI LAin)8.
Every one in Nebraska will sooner or later hear of the so-ealled alkali
lands. They are not confined to any one geological fiHmatioD, but are
foAud sometimes on the Drift, Alluvium, or the Loess. They increase in
numbcff ftom theeastern to the western portions of the State. Yetone-half
of the counties of the State do not have any such lands, and often there
are only a few in a township or county. Where they have been doeely
AU6HET.]
NEBRASKA — THE BAD LANDS.
"261
examined they are fo'nnd to vary a great deal in chemical oonstitnents.
Generally, however, the alkali is largely composed of soda compound:^,
with an occasional excess of lime and magnesia or potash. The follow-
ing analysis of these soils shows how variable they are. The first is
taken from the Platte bottom, sooth of North Platte ; the second from
near old Fort Kearney, and the third two miles west of Lincoln.
Ini^luble (slllceoiu) matter
Ferris oxid«
AlomiDa
Ijime, carboDAte
JAme, ptaotpbate
Ma^eida, carbonate
Pota»h
Soda, carbonate and bicaiboaate
Sodinm, ralpbate
Sfointore
Organic matter
LosNin ADoljiiU
74.00
3.f)0
2.C8
6.01
1.70
1.89
1.68
!kl7
.70
.99
l.SO
.78
106.00
73.10
3.73
8.89
4.29
1.40
1.39
1.80
7.33
.89
.98
8.10
.80
loaoo
73.90
3.69
8.10
3.90
1.49
1.47
3.69
4. 91
.89
.98
8.10
.88
loaoo
The specimens for analyse were not taken from soils crasted over
with alkaline matter, bat from spots where the ground was covered
with a sparse vegetation.
Many of the alkali lands seem to have originated from an accumu-
lation of water in low places, where there is an excess of alamina in
the soil or snbsoil. The escape of the water by evaporation left the
valine matter behind, and, in the case of salt (sodiam chloride), which
all waters are known to contain in at least minute qaantities, the chlo-
rine, by chemical reactions, separated from the sodium ; which latter,
uniting immediately with oxygen and carbonic acid, formed the soda
compounds.
These alkali spots are often saccessfaily cultivated. The first steps
toward jtheir renovation must be drainage and deep cultivation. The
Bext step is the consumption of the excess of alkali, which can be
effected by crops of the cereal grains in wet seasons. In such seasons
these alkali lands, if deeply cultivated, often produce splendid crops of
grain. Wheat is especially a great consumer of the alkalies; axid these
being partly removed in this way, and the remaining excess mingled
with the deeply-cultivated soil, renders it, in many instances, in a few
years capable of being used for the other ordinary crops of Nebraska.
Treated in this way, these alkali lands often become the most valuable
portions of the farm. There are comparatively few alkali lands in the
State that cannot be reclaim^ in this way.
THE BAD LAJB^DS.
The bad lands do not really belong to the surface-deposits, as they
constitute a peculiar formation, where most of the soil capable of being
cultivated has been removed by denudation. As they, however, comprise
nearly all that there is of the surface in a part of the northwest 45orper
of the State, they deserve mention in this place. They are mostly found
between Spoon Hill Greek and the Niobrara Biver, and they extend
down from the White River in Dakota Territory. They belong to what
Hayden calls the White River group of Tertiary rocks. They are be-
lieved to be of Miocene age. This region has long been known as the
bad lands — mtmvaises terresj or, in the Dakota language, ma-koo-H'tchay
which means a difficult conntiy to travel, because the sur&ce is very
broken, and there is little, if any, good water, wood, or game.* The
' Hayden United States Geological Survey, 1870.
262 GEOLOGICAL SUBVEY OF THE TEEBITOBIES.
materials of the deposits are white and yellowish indurated clays, sands,
marls, and occasional thin beds of lime and sand stones. When going
through these bad lands, I observed these lime and sand stones to appear
and disappear in the most unexpected manner, indicating great variety
in the conditions under which they were formed. The world is indebted
to Hayden for investigating and making known these wonderful beds.
His descriptionsof them are correct in every particular; and yet it is hard
to realize their grandeuranduniquenesswithout personally visiting them.
This, at least, was the case with myself. The geologist never tires of in-
vestigating these deposits and their curious remains. The almost ver-
tical sections of variously^cotored rock have been chiseled by wat^
agencies into unique forms. Indeed, viewed from a short distance they
remind the explorer of one of those old cities which only exhibit their
ruins as reminders of theirancient greatness. Among these grand deso-
lations the weird, wild old stories of witchery appear plausible and pos-
sible. It is in the deep caiions at the foot of stair-like projections that the
earliest of those wonderful fossil treasures are found which have done
so much to revolutionize our notionsof the progress of life and of Tertiary
times. In the lower beds of this deposit are found remains of Ehinoceri
and Hyppopotami^ which were river-horses much like the Hpppopotamiof
modern times. Higher up in the deposits are found countless numbers of
turtles, mingled with the remains of land-animals, i was especially
amazed at the number of these turtles in a light reddish-coloreil marl-
bed. They seemed in a few localities to constitute almost the entire de-
posit. Among these animal-remains none are more curious than the
Oreontid(ej which Leidy calls ruminating hogs, because their cutting teeth
and canines and their t^t were like those of the swine family, while
their molars were patterned after those of the deer, and the upper por-
tions of the head much like that of the camels. According to Hayden,
they existed in great numbers of species and individuals, and con-
gregated in great herds, like the buffaloes in their palmy days. Here
also are found the remains of many species of horses and a few camels,
a beaver, &c. The vast numbers of these animals were kept within
bounds by gigantic carniverous animals, such as saber-toothed tigers,
Hyaenodons^ foxes, wolves, &c.
Agriculture in such a region as this, where often nothing is now grow-
ing is, of course, out of the question. Whether there ever will be such
an increased rain-fall as to start vegetation in this region and make its
surface capable of cultivation, is a problem of the future. Regions as
rough have been cultivated by hand. Here some of the deposits, like
the marls, possess the elements of fertility in a high degree, butmoisture
is entirely lacking. Though this region is so unattractive to the utilita-
rian, 1 doubt whether any other equal area of Nebraska will be of more
benefit to mankind, simply because here we have outlined so marvelonsly
the old life of Miocene times, and it must ever be a stimulus to geologi-
cal studies, and those grand results which scientific culture produces.
Na novel can be as interesting to a thoughtful mind as Hayden's descrip-
tions of these bad lands and their animal remains.
FUEL FROM THE 8UBPAOE-DEPOSITS.
It is not yet absolutely settled how much dependence can be placed
on the coal-supplies of the Carboniferous, Cretaceous, and Tertiary de-
posits, in each of which thin beds have been found and worked to a
limited extent. Hayden and Meek incline to the opinion that no beds
of coal thick enough and of sufficiently good quality to be profitably
AUOHET.] FUEL FROM THE SURFACE-DEPOSITS. 2 63
worked will be fonnd in the State. (Hayden's Report for 1870, p. 134, &c.)
There is, however, do qoestion aboat the great quantity of peat in Ne-
braska. Hay den mentions many localities where it is found. (Report for
1867, 1868, and 1869.) It is also found on the tributaries aud head-
waters of the Logan, the Eikhorn, the Blue, and on Stinking River, and
other tributaries of the Republican. One peat-bog ou the Ix)gan (town-
ship 28 north, 1 and 2 east) is five or six miles in length and of vari-
al>le breadth. I could find no bottom to this bog with a fifteen-foot
|K>]e. This peat I personally tested and found to be of excellent quality.
In fact, nearly all the peat that I have tested in the State is fully up to
theaveragein quality. A singularly good article is found at Pittsburgh,
on the Blue River, where tbe deposit is also quite extensive. Among
the animal-remains submitted to me for examination from this bed was
u molar tooth of the gigantic beaver {Castor ohioeMis), proving that this
animal existed in Nebraska in times geologically recent. The most of
the peat-beds that I have examined seem to have been formed in lake-
lets that gradually became bogs by an accumulation of vegetable mat-
ter derived irom coarse grasses, sedges, rushes, polygonums, duck- weeds,
pond-weeds, arrow-weed, &c., lilies, &c. Sphagnum, which seems to
form the mass of organic matter in peat-bogs oF granitic and siliceous
diatricts, only occurs in Nebraska in a bog near Curlew, in Cedar County,
and one or two other places in the same region. At legist I found it no-
where else. Many of these peatbogs are now so far advanced as to be
dry enough to be wagoned over in midsummer, but through the mid-
dle of which a stream of water is still flowing. Others have no visible
outlet, but retain the water poured into them, when the spring and June
rains fall, during the remainder of tbe year, and thus supply the condi-
tions necessary for the peculiar vegetation of such formations. Some-
times, too, depressions in the surface where peat is forming are supplied
with moisture from ever-flowing springs. The beginnings of many of
these peat-beds date back at least to the close of tbe Loess age, so
that sufficient time has elapsed for the accumulation of great quanti-
ties of this material. Peat can be cheaply taken out of a bog with a
spade, and laid up like cord-wood under cover to dry, when it is ready
for use. The objections to using it thus prepared is its liability to crum-
ble. Unfortunately, to prepare it by molding and pressing requires
some capital for apparatus, and this is one reason why these beds have
not yet been worked. In some places, too, wood-fuel is yet cheap, and
in others coal irom abroad is easily obtained, and these causes have also
operated to delaiy the use of peat for fuel. But such treasures cannot
remain unused forever. Eventually this peat must be utilized, and, if
it is cheaply furnished, as it can be, the State will be supplied for a long
time from its own territory for manufacturing purposes and domestic
use with all the fuel needed. (For an able discussion of peat in Ne-
braska, see Hayden's Final Report of Geological Survey of Nebraska,
p. 69.)
WATER BESOUBOES OF NEBRASKA*
•
Running streams are an evidence of tbe degree of moisture in a region,
and with these Nebraska is well supplied. Any good map of the State
will show numerous rivulets flowing into the larger creeks and rivers.
But no map that I have yet seen does or can do full justice to the num-
berless small streams that are found in the State. Having traveled, as
a naturalist and explorer, over a large part of Northern Nebraska, I fre-
quently came across small streams with beautiful bottoms, where even
the published plats of the public surveys failed to indicate them. In
264 GEOLOGICAL SURVEY OP THE TEERIT0BIE8.
fact, there arc large areas of the State where ranniiig water can be foand
on every section, and often on every quarter-section of land. Where
SQch water resources do not exist, it can easily be obtained by digging
or boring to a certain depth. In the Loess deposits water is treqaently
found at a depth of from fifteen to forty -five feefc. If this proves a fail-
ure, as it occasionally does, water can be obtained beneath, in the
Drift ; or, where this is absent, when the underlying rocks are reached.
At the bottpm of the Loess deposits there is generally a layer of sand or
gravel, which is a great reservoir of water, and from which it flows in
unlimited quantities. In some of the counties drained by the Blue Rivers
and their tributaries, but rarely east of them, where the Loess deposit8
are very thick, wMev is not found until this stratum of sand and gravel
is struck, at a dept h of from sixty to one hundred and twenty feet. I
have known of only a few instances where the underlying rocks had to
be penetrated to secure x>ermanent water. This underlying bed of sand
and gravel is, as before observed, ))robably Drift, and exists, at some
depth, over the greater part of the State. An interesting phenomenon
connected with the Platte and Republican Rivers is the drainage of a
portion of the waters of the former into the latter. The Platte flows
eastward, at a considerably higher level than the Republican, and be-
tween the two rivers there is- a large area of Loess, underlaid by Drift,
sand and gravel, which in many places is continuous between the two
rivers. Through this Drift, sand and gravel the waters of the Platte,
where they run over it, flow into the Republican. The two rivers are,
in the main, parallel, and, at the meridian of Kearney Junction, are only
forty miles apart. In traveling along the Republican for a hundred
miles, from Orleans westward, and by wading in the river for miles at a
time, I observed such a quantity of water trickling through these sands
near the water's edge, iu hundreds of places, that it could not possibly
all have come from the superficial deposits It was during the dry sea-
son (August) of 1874 that I made these examinations. Occasionally,
where this underlying bed of sand and gravel lies on clay or rock, 8ni>-
terranean currents are formed.
At a distance from running streams it is found, by exi)erience« to he
cheapest and best to supply water to stock and for domestic use by
sinking a shaft to the Drift, where water is found, and working the pump
by a wind-mill. One such at Ball's ranch, on the road between Kear-
ney and Orleans, had the tank kept full by a windmill, and furnished,
as I was informed at the place, water for four hundred cattle and other
stock, the traveling public, and for domestic use. The well here was
one hundred feet deep, ninety of which passed through Loess deiiosits.
Half a dozen small farmers often might unite to dig such a well, and to
supply it with a windmill, near the intersection of their lands. This
would be especially advantageous in the region between these two riv-
ers, west of the meridiau/of Kearney, where the subsoil is Loess, and
very thick; where running streams are few, and where wells must be
sunken deep to reach permanent water.
t3hemical analyses show that the waters of the State, excepting the semi-
alkaline ponds in some sections, is fully equal to the average in parity.
The most common foreign ingredient is lime carbonate. I have fie-
quently examined wells whose waters were charged with being impure,
and in every instance found that the impurity was caused by the pres-
ence of organic matter that had been permitted to be washed in from
the surface. A correction of this defect soon purified the well.
An interesting meteorological fact, having an important bearing on
geological causes, is the increase of rain-fall all over the State, as eivili-
AUOBET.] TIMBER IN MODERN GEOLOGICAL TIMES. 265
zation advances westward. As early as the snmmer of 1865, 1 examiDed
the region at the headwaters of the Logan, Elkhorn, and Bow Bivers,
where I found many small ancient creek-bottoms, with stream-beds in
the center, or nearer one side, all grown over with a thick sod of grass
and ^"eeds, and where the water had not flowed for ages. To be sure of
this conclaaion, I dug down, at convenient places, to ascertain the condi-
tion of the subsoil. In almost every instance I found more or less shells
of fresh-water mollnsks, so decayed that on the least exposure they
would crumble to pieces. They all belonged to the genus Vnio or Ana-
dontaj the former seemingly being most abundant, but this probably
resalted from the greater fragility of the latter. I failed to identify any
species. Many of these localities I had marked. Already in 1871 many
of these old streams commenced again to flow, and since then many
more have become supplied with apparently permanent water. Many
apriogs of water, too, are bursting out along bluffs where nothing of the
kind was known before. It is probable that the great amount of land
broken up and cultivated absorbs more of the falling rains than could
have been taken in by the hard prairie. Let any one carefnlly watch a
slope, one-half of which is plowed deeply, and the other half yet virgin
prairie, during a heavy rain ; the former will absorb all the water that
iJEiUs, while it runs off the latter in currents. The constant evaporation
of this increased water-supply must, in the nature of the case, produce
more vapor in the atmosphere. In my opinion, however, we may ac-
oouat for it. There is little room to doubt tliat the atmosphere is becom-
ing more moist or the rain-fall is increasing, or both, all over Eastern
and probably Western Nebraska. The great change constantly going
on in the flora of the State points jb^ the same conclusion. The grasses
especially and the sedges characteristic of dry regions are rapidly re-
treating, and in many places disappearing altogether, while others, that
are more peculiar to moister regions, are taking their places. Hayden,
irom a most careful study of a partially different clasA of facts, long
since came to a similar conclusion. (See his report for 1870, p. 455, &c.)
TIMBEB IN MODEBN 0EOLOGIOAIi TIMES.
It is natural to suppose from well-known natural causes that when
the Loess age was drawing to a close, and the lower portions of the area
covered by these deposits was yet in the condition of a bog, the climate
was much more favorable than the present for the growth of timber.
Bainfall and moisture in the atmosphere must then have been much
more abundant. In July, 1868, while walking along the edge of one of
the Logan peat-bogs in Cedar County, my jacob-staff struck some hard
body in the peat. Examining it more closely I found a log buried in
the peat at least sixty feet in length. Following up this discovery with
a careful search, I found in this and other bogs a great many buried logs
of various length and thickness. Most of them were found where there
was no existing timber within twenty miles, and from which they could
not have floated in flood-times. I regret that I had no means of extri-
cating some of those logs, and ascertaining the species to which they
belonged. That would no doubt have thrown much light on the changes
that have taken place since they were buried in the bog. But they evi-
dently grew on the shores or banks, and after falling into the bogs they
were protected against decay by the well-known antiseptic properties of
peaty waters. Another fact that shows the greater prevalence of tim-
ber within geologically recent times is the remnants of old pine-forests
3ret buried in the ground. In the summer of 1868, when traveling Rlong
266 GEOLOGICAL SURVEY OP THE TERRITORIES.
and near the Niobrara, roots of piue trees were often foand sticking in
the ground, more than fifty miles sonth and east of the present forests
of this timber. Often did these old roots famish me with the materials
of a camp fire. At no very remote period pine forests must have floor-
ished down to the month of the Niobrara. Many other facts, of a simi-
lar character, seem to leave no room to doubt that in geologically recent
times far more extensive forests prevailed all over Nebraska than those
which now occupy the ground. What caused their disappearance can,
perhaps, not be certainly determined. Some geologists hold that the
increasing dryness of the climate caused the disappearance of any old
forests that might have existed. But might not the converse of this
also have been true here, as well as elsewhere, namely, that the destrae-
tion of forests inaugurated the dry climate that prevailed when this ter-
ritory was first exploreil f It is at least conceivable that the primitive
forest received its death-blow in a dry summer by fire, through the van-
dal acts of Indians in pursuit of game or for purposes of war. What
suggested this theory as a possible explanation of the disappearance of
forests on this territory, was the finding of the pine-roots before referred
to, and often, when partially buried, showing marks of fire fiLX>m carbon-
ized ends, and in localities so sandy, and Where vegetation was so scant,
that an ordinary prairie-fire was out of the question. An old tradition,
that I once beard from the Omaha Indians, points to the same condn-
sion.
It is wonderful how nature here responds to the effort of man for re-
clothing this territory with timber. Man thus becomes an efficient agent
for the [)rodnction of geological changes. As prairie-fires are repressed
and trees are planted by the million, the climate must be still further
ameliorated. When once there are groves of timber on every section
or quarter-section of land in the State, an approach will be made to
some of the best physical conditions of Tertiary times. The people of
this new State have a wonderful inheritance of wealth, b^sauty, and
power in their fine climate and their rich lands, and as they become con-
scious of this they will more and more lend a helping hand to the pro-
cesses of nature for the development and utilization of the material
wealth of Nebraska.
MOLLUSKS IN THE LACUSTRINE DEPOSITS.
The following list of land and fresh-water shells comprise all that I
have thus far identified, in whole or in p»rt, from the Lacustrine deposit8.
Nearly all are extremely fragile. The Hyalinas, Pupas, and some of the
Helices long eluded my efforts at identifying them. I finally marked
the localities where found until the ground was frozen, when they were
cutout with a knife. They were then identified by making thin sec-
tions with a sharp knife. Many of these moliusks, after being placed
for a while in my cabinet, fell to pieces. For this reason, I have no
specimens to show of many species here given, and, therefore, only pre-
sent this as a provisional list. Some well-preserved s{>ecimeD8 appear
to me to be new to science, but as I have not access to the descriptions
of the new species discovered by Hayden, a bare list of which is given
in Binney and Bland's Land'and Fresh Water Shells, I will not ven-
ture to describe them, as that has probably already been done. The
counties are indicated where the specimens were obtained, or where
they were the most abundant:
Vitrina limpida Oould, Lancaster and Dixon Counties.
Hyalina nitida f Muller, Dixon County,
ALOHKT.l MOLLUSKS IN THE LACU8TBINE DEPOSITS. 267
Hyalina arhorea Say, Douglas and Dakota Counties.
Hyalina viridula Monke« all Eastern Nebraska.
Hyalina indentata Say, Otoe and Douglas Counties.
Hyalina limatula Ward, Douglas County.
Hyalina minuscula Binney, all Eastern Nebraska.
Hyalina binneyana t Morse, Dixon and Cedar Counties.
Hyalina ferreaf Morse, Dixon County.
Hyalina exigua Stimpson, Dixon and Cedar Counties.
Hyalina intertexta f Binney, Douglas County.
Hyalina ligera Say, Otoe and Nemaha Counties.
Hyalina demissa t Binney, Nemaba and Richardson Counties.
Hyalina fulva Drepamaud, Dixon and Cedar Counties.
Hyalina la»modon Phillips, Nemaha and Otoe Counties.
Hyalina interna Say, Nemaha and Otoe Counties.
Hyalina significans Bland, Nemaha and Otoe Counties.
Hyalina lineata f Say, Douglas and Otoe Counties.
Macrocyclis eoncava Say, Douglas and Otoe Counties.
Helix solitaria Say, Otoe and Burt Counties. •
Helix strigosa Gould, Otoe and Burt Counties.
Helix alternata Say, all Eastern Nebraska.
Helix oumberlandiana Lea, Middle Lacustrine in Nemaha and Otoe
Counties.
Helix cooperi W. O. B., Douglas and Washington Counties.
Helix striatella Anthony, Dixon and Dakota Counties.
Helix Idbyrinthica Say, all Eastern Nebraska.
Helix hubhardi Brown, Middle Lacustrine in Nemaha County.
Helix auriforniis Bland, Middle Lacustrine in Otoe County.
Helix tholu^ f W. G. Binney, Middle Lacustrine in Douglas County.
Helix fastigans L. W. Say, Middle Lacustrine in Otoe County.
Helix Jcu^ksonii t Bland, Middle Lacustrine in Otoe County.
Helix hazardi f Bland, Middle Lacustrine in Douglas County.
Helix dorfeuilliana Lea, Middle Lacustrine in Cass County.
Helix pu8tulaf Fer, Middle Lacustrine of Cass County.
Helix spinosa Lea, Middle Lacustrine of Harlan County.
Helix edgariana t Lea, Middle Lacustrine of Richardson County.
Helix atenotrema Fer, Otoe and Cass Counties.
Helix hirsuta Say, Dixon and Cass Counties.
Helix inonodan Ruckett, all Eastern Nebraska.
Helix palliata Say, all Eastern Nebraska.
Helix absiriotaf Say, all Eastern Nebraska.
Helix appreasa f Say, Otoe and Nemaha Counties.
HeUx inflecta Say, all Eastern Nebraska.
Helix tndentata f all Eastern Nebritoka.
Helix fallax Say, all Eastern Nebraska and Republican Valley.
Helix albolabria Say, Eastern Nebraska and Republican Valley.
Helix multilineata Say, all Eastern Nebraska.
Helix pennsylvanica Green, Douglas County.
Helix elevata Say, Eastern Nebraska and Republican Valley.
Helix ex0leta Binney, Eastern Nebraska and Republican Valley.
Helix roetneri Pleifer, Middle Lacustrine of Richardson County.
Helix thyraideH Say, Eastern Nebraska and Republican Valley.
Helix ciausa Say, Eastern Nebraska.
Helix jguna f Say, Richardson County.
Helix profunda Say, all Eastern Nebraska and Republican Valley.
Helix pulchelUi MUU., all Eastern Nebraska and Republican Valley.
Helix , Republican Valley
268 GEOLOGICAL SURVEY OP THE TERRITORIES.
Helix , Otoe and Nemaba Coanties.
Helix , Otoe and Keuiaba Counties. ,
Helix , Otoe and Nemaha Oonntiee.
Helix , Dakota and Dixon Oonnties.
Helix , Dakota and Dixon Counties.
Bulimulus dealbatus Bay, Middle Lacastrine of Nemaha Connty.
Cionella subcylindrica Linn., Southeastern Nebraska.
Fupa muscorum f Linn., Cedar Connty.
Pupa blandi Morse, Dixoo, Dakota, and Burt Counties.
Pupafallax Say, Dixon, Dakota, and Burt Counties.
Pupa armi/era Say, all Eastern Nebraska.
Pupa corticaria Say, all Eastern Nebraska.
Succinea hoydenif W. G. B., Republican Valley.
SucciTiea mooresiana Lea, Republican Valley.
Succinea avara. Lea, Republican Valley.
Succinea ohliqua^ Say, Dixon and Dakota Counties.
Succinea , Otoe and Nemaha Coanties.
ZonUes fuliginosaj Griif., Republican Valley.
Zonites Icevigata f Pfeifter, Republican Valley.
Zonitea inornata^ Say, Cass and Otoe Counties.
Zonites gulariSj Say, Southeastern Nebraska. *
Carychium f exiguum t Say, Nemaha County.
Limncea stagnalis t Linn., Washington County.
Limncea replexa Say, Dakota and Dixon Coanties.
Limncea palustris MlllL, along Missouri Bluffs.
Physa gifHna Say, Dakota Connty.
Physa lieterostropha Say, Doaglas County.
Phyaa , Doaglas County.
Physa , Douglas County.
Psulinus , Otoe County.
Planorbis glabratus Say, Otoe County.
Planorbiscampanulatus Say, Dakota County.
Planarbis corpulentus f Say, Dakota County.
Planorbis deflectus Say, Nemaha County.
Planorbis allmsf Miill., Dixon County.
Ancylus , Dakota, Harlan Connty.
Valvata tricarinata Say, Dixon County.
Valvat4i Say, Otoe and Burt Counties.
Vivipara intertexta f Say, Otoe County.
Vivipara subpurpurea f Say, Otoe and Nemaha ConntieB.
Vivipara contcctoides Binney, Nemaha County.
Melantho ponderosa Say, Washington County.
Melantho decisa Say, Burt County.
Amnicola perata f Say, Washington County.
Amnieola lemnosa f Say, Washington County.
Pomatiopsis lapidaria Say, Dakota Connty.
Helicina orMculata Say, Nemaha Couiity.
Angitrema armigera Say, Nemaha County.
Lithasia obovata Say, Richardson Connty. *
Pleurocera undulatum t Harlan County.
Pleuroeera caaialeoulatum Say, Nemaha County.
Pleurocera elevatum Say, Otoe Connty.
Pleurocera labiatum f Lea, Richardson County.
Pleurocera simplex f Lea, Otoe Connty.
Chniobasis depygis Say, lUchardson and Otoe Counties.
Ooniobasis livescensf Menke, Richardson Connty.
AUGHRTj MOLLU8K8 IN THE LACUSTRINE DEPOSITS. 269
Go7iiobasi^ brevispira f Anthony, Otoe County.
OoniobasU semicarinata Say, Otoe Goanty.
A^ncttlosa costata Anthony, Bichardson Goanty.
A^nculosa praerosa Say, Eicbardson County.
A^nculosa f , Eicbardson County.
Unio , Cedar, Dakota, and Burt Counties.
Unio , Neuiaha County.
Unio , Otoe and Cass Counties.
A^nadonta , Washington County.
Anccdonta , Eepublican Valley.
1
\
PALEONTOLOGY.
REPORT OF LEO LESQUEREUX.
S71
Columbus, Ohio, March 7, 1876.
Dear Sm: I send yoa herewith, on the fossil floras of the western
Territories, a record of the progress and discoveries in this section of
the !North American natural history, since the publication of the last
annual rei)ort for 1873.
The memoir is divided into two parts. The first' refers again to the
evidence afiforded by fossil plants to the age of the lignitic formations,
and describes the species not yet known from former communications.
The second critically reviews the Cretaceous flora of the Dakota group,
and describes also, with figures, the new materials obtained from this
remarkable formation. This revision was demanded not ooly by the im-
portant discoveries 'Which have enriched this flora, but especially by the
kind criticisms of European authors and the great interest with which
the publication of the (3retaceous flora has been received by geologists.
Very respectfully, yours,
L. LESQUEREUX.
Prof. P. V. Haydbn,
United States Geologist^ Washington.
18 H
373
ON THE TERTIARY FLORA OF THE UORTH AMERICAN UGNITIC,
CONSIDERED AS EVIDENCE OF THE AGE OF THE FORMATION.
/
The parpose of this memoir, as indicated hy the heading title, is to
present, with more details, the evidence offered hy the flora of the Lig-
nitic Measures of the West, in regard to the geological age of their for-
mation, which I consider as Tertiary. The reasons advanced in favor of
this opinion in the two former annual reports of Dr. Hayden, and in a
paper in the American Journal of Science and Arts,* are controverted by
some geologists who consider the Ligui tic as Cretaceous, denying to vege-
table paleontology the authority of evidence in a question of tbis kind.
Their arguments may be bri^y exposed in the order iq which I propose
to examine and discuss their importance.
1st. Fossil plants are rarely lound in the geological formations which
are mostly marine ; the vegetable remains are generally undetermina-
ble fragments of leavejs } they have been, as yet, scarcely studied in this
country ; the records of the fossil floras are nearly mere blanks.
2d. If even the fossil flora of the great Lignitic of the West had been
widely studied, it could not afford any reliable evidence, on account of
the impossibility of a conclusive comparison of its species. A compari-
son of the fossil plants of this continent with those of Europe can ])rove
nothing in regard to identification of geological periods, for the reason
that at the same epoch the floras of both continents may have been far
different in tbeir character, a necessary result of differences in their
atmospheric circumstances of the same period of time.
3d. Even supposing that the evidence could be admitted, it is put at
naught by the presence of cretaceous animal remains in strata within or
above the lignitic formations, and animal remains must have priority
for the determination of geological groups.
4th. The strata of the Lignitic conformably overlie the Cretaceous, and
the nature of the compounds of these so-called different formations are
similar.
5th. Stratigraphy and animal paleontology have forced the conclu-
sion in regard to the cretaceous age of the western Lignitic, and geolo-
gists of high standing have, by their opinion, given full authority to
this conclusion.
The text of the argumentation in favor of the cretaceous age of the
Lignitic is here exposed in the fairest possible way. It could be said
merely that the objections have been already considered and answered,
but nobody would be satisfied or enlightened by this assertion. It is,
therefore, advisable to reconsider the subject and to expose, instead of
contradicting arguments, facts, which, corroborating former assertions,
bring some new light upon the controverted question. For, in the two
'Annual Report of the United States Geological and Geographical Survey, &c., for the
explorations of 1872, p. 318, &c Same Keport for explorations of 1873, p. 367. On the
age of the lignitic formations of the Rocky Mountains, American Journal of Science and
Arts, vol. Yii, June, 1874.
S75
276 GEOLOGICAL SURVEY OF THE TEBBITORIES.
past years, the researches in the vegetable paleontology of the Lignitic
have greatly added to what was known of its domain when the former
reports were published.
To consider the first objecUon'^that fossil plctnts are rarely found tn
the gmlogical formations which are mostly marine; that the vegetable remaiiis
are mostly undeterminable frojgments of leaves ; ikat they have been as yet
scarcely studied ; and that the records of thefossU floras are mere hlanki- —
it will be necessary to open a while these so-called.blank records of oar
North American geological floras and look over them a little.
We cannot boast, indeed, of a wide acquaintance with the fossil plants
of the Silurian, for the good reason that they have been rarely looked
for and studied. The formations of that epoch being mostly marine,
their flora is represented by fucoidal remains, or plants which, originally
of a soft texture, have generally been deformed and rendered undetermi-
nable by maceration and compression. Prof. James Hall has, however,
described some of those primitive vegetable forms, and his contribn-
tions to the vegetable paleontology of the Silurian have been acknowl-
edged and honorably recorded by European authors. Of the twenty
species of Silurian plants described by Goppert in his Flora of the For-
mations of Transition, sixteen are credited to the authorship of Hall.
Besides the general instruction afforded by the representation of
those plants of primitive ages, we find in them already, though uncer-
tain theircharacters may be, an authority for the identification of Silurian
strata in far distant countries. It is the case, for example, with Die-
tionetna flabelliforme^ Hall, Eich., which identifies, by its abundant re-
mains, the Lower Silurian of Norway and of Bohemia, &c., the Lingnla
flags of England, Ireland, and the strata of the same age, the Potsdaai
epoch of the United States and Oanada.
As I have merely to consider the remains of land-plants, the whole
Silurian flora might be left out of notice as foreign to the subject. Bat
even land-plants have their history, 'at least the first lines of it, writ-
ten in those Silurian formations, considered till now as a succession of
marine deposits, as a time when our planet was surrounded by water,
and when as yet there was no land exposed to view. Two years ago a
few stems or branches were found in beds of hard clay of the CinciuDati
group of the Silurian, near Lebanon, Ohio. They were, after examina-
tion, considered as remains of land-plants, and as representing upon
their surface the impression of scars as a species of SigiUaria. This
opinion, which was then contradicted, is now fully confirtned by a new
and more careful examination, made by competent judges, who admit
that the remains in question can represent only land-plants. We conid,
therefore, chronicle the presence of land covered with vegetation as far
down as the Middle Silurian, if we had positive evidence concerning the
origin of these remains in the locality indicated by their labels. It is,
indeed, supposable that those fragments may have been found some-
where else, and have been casually mixed with specimens of the Cin-
cinnati group, though the place of origin is positively known and vouched
for by the owner of the specimens. The presence of land-plants in as
low a member of the Silurian receives, however, a degree of probability
from the recent discovery of remains of two species of this kind in the
Lower Helderberg of Michigan. Here no doubt is left either in regard to
the character of the plants, which are clearly exposed, or to the locality
and its reference to the formation.* One of the species is a small
Fsylophiton ; the other belongs to the genus Annulariaj but is evidently
* This diacoyerj is dne to Dr. Boeminger, S^ate geologist of Michigan.
I.E8QUEREIX.1 EVIDENCE OF AGE OP LIGNITIC GROUP. 277
new, and of pecaliar characterR. Both were p^rowing together, apparently
in the plaee where they have been found, as they are inhabited by a
small flovial or land shell, a serpnlid, very much like the Spirarbis so
commonly observed upon coal-plants of the Carboniferous. This shell
is still smaller, and without the transverse strisB observable upon the
8X>ecies of the Coal-Measures.
The conclusion in regard to the presence of land-vegetation in the
Silurian had been already recorded by Professor Dawson, but less posi-
tively ascertained, however.* He remarks that in the marine lime-
stone of Cape Gasp6, holding shells and corals of Lower Helderl>erg
age, they have fragmeutal stems and distinct rhizomes of FsHophitum^
adding that these fragments must have been drifted from the land. In
the present case, or with the vegetable remains of Michigan, the frag-
ments are so delicate, their minute divisions so well preserved, that evi-
dently their habitat was in close proximity to the place where they have
been found, or rather that they lived in shallow b8.8ins of water border-
ing the shores, this being especially indicated, as remarked above, by
numerous small fluvial mollusks, either placed upon the plants, or scat-
tered around upon the stone.
Remains of this kind, evidence of open land in the Upper Silurian age,
may be hereafter more frequently recorded and found also still lower in
this formation when more care is given by geologists to the collection
and examination of fossil plants. Though it may be of the future, these
fragments of old lycopodiaceous species in the Silurian appear there as
the ancestors of a long and multiple scries of analogous forms, all re-
markably well characterized, and which, from the Lower Devonian, in-
crease in a remarkable proportion to the base of the Carboniferous,
where their remains enter for a large proportion into the composition of
the coal.
The list of the Lower Devonian plants is not as yet very long. But it
is a matter of course, for the strata of this formation, at least in the
United States, are mostly marine, and the fossil vegetable remains in
connection with them represent marine plants which have been till now
scarcely studied in this country. That they are very abundant, is proven
by the fact that they have become by their presence noticeable characters
of whole geological epochs to which they have given their name, as for
example, Fuccides CaudaOalliy for the C)audarg^li grit, the lower mem-
ber of the Corniferous period.
Marine plants, though admirably beautiful they may be, some of
them at least in their living state, have nothing attractive as fossils.
Their fronds and branches are generally flattened by compression, and
in that way, too often disfigured and generally mixed into an amor-
phous mass, where the e.ves rarely discern any trace of orgiiuization
or of coniiguration acceptable as reliable characters. The paleontologist,
therefore, needs for the study of these plants the greatest 4;are and a Ikrge
number of specimens, which are rarely obtainable; for the plants and
their ramifications either cover wide surfaces of hard rock, or penetrate
it in various directions. I believe, however, that with time and perse-
verant researches, paleontologists will be able to determine a number of
those obscure remains, and point out by their presence tbe distribution
of some separate groups of the Devonian. But this subject is out of tihe
present discussion.
There is in Canada a great sandstone formation known as the Gasp^,
over seveu thousand feet thick, ^hich has few animal remains in its
* Fossil Plants of the Devoniaii and Silarian Formation of Canada, pamphlet (1871), p. 78.
278 GEOLOGICAL SURVEY OF THE TEBBITORIES.
compounds, and wbose geological relation has never been satisfactorilj
determined either by stratigraphy or by animal paleontology. Professor
Billing refers its lower part to the Oriskany sandstone of New York,
withont positive evidence, however; its middle part is donbtfally con-
sidered by Professor James Hall as representing the Hamilton groap.
Taking into consideration thedata supplied by fossil plants whose remains
have been found from the base to the top of this formation, Professor
Dawson finds that they represent a succession, by multiplication of spe-
cific or generic forms, of the whole devonian flora, as far as it is known,
till now, and that therefore this enormous accumulation of sandstone
has been in constant process of formation during a whole epoch, expos-
ing in its successive strata the gradual development of its vegetable
types. Its divisions are not as yet positively defined by the celebrated
professor of Montreal. But surely a more detailed study of the distri-
bution of the species of fossil plants of the Ga8p6 will enable the paleon-
tologist to fix, by the grouping of related forms of plants, the different
stages of the devonian land formation, and thus afford points of com-
parison for future researches.
This we can do distinctly for the Carboniferous age, taking as its
beginning or its base the Old Red Sandstone, represented in this country
by the Catskill period. In the Upper Chemung, wehave here, as in Canada
and in England, some few remains first representatives of a peculiar
group of ferns, whose characters have no relation tothoseof any species
of our time. Its species have been described by the authors under vari-
ous generic names. They are referred to Cyclopteris or Adiantit&t by
some ; to Noeggerathia or Spkenopteris by others 5 to Arckeopteris or Fale-
opteris in more recent works. This multiplication of generic names
does not refer to uncertainty of characters. Every paleontologist
knows these plants ; but their undefined analogy has forced different
points of view in regard to their relation, and therefore caused this
confused terminology. These ferns, from their rare presence in the De-
vonian, become so predominant in the red shale of the Catskill period
of this country, and of the Old Red Sandstone of Europe, that they are
considered as characterizing the formation by their remains. This fact
is acknowledged even by geologists who do not take any account of
vegetable paleontology. The more common species of this group of
ferns — Faleopteris hyhernica^ P. RoeTneri^ P. Boscii^ described first irom
the Red Sandstoneof England, are represented in the red shale, Nos. ix
and X of the Pennsylvania geological reports, (the Catskill,) below Potts-
ville, Manch Chunk, and other places. Paleopteris Malliana and P. Jack-
8oni are American species of the same tpye. In Europe two species, P.
Reussii & P. unequilateralis, ascend to the Sub-Carboniferous limestoue,
and here also, as will be remarked below, we have two species known
already in the next higher stage of the Carboniferous. Therefore the
predominance in the Catskill bedsof a group of plants which is still rep-
resented by a number of species at a higher stage of the Carboniferous,
marks its place with the last geological divisioil rather than with the
Devonian. These Paleopteris species, like those of Megalopteris men-
tioned in the followijig division, have often been considered as Devoni-
an types ; this, apparently, because the Old Red Sandstone has been often
and is still sometimes admitted as Devonian. All the European species
described are referred to the Old Red or to the Culm, or Sub-Carbon-
iferous ; those of Canada to the upper beds of Gasp6, a formation which,
as remarked already, is not yet limited in its divisions, and may repre-
sent the Catskill by its upper members.
To this lower member of the Carboniferous are referable a number of
LE8QUKREUX.] EVIDENCE OP AGE OP LIGNITIC GROUP. 279
species of plants described by Prof. B. F. Meek, in proceedings of the
Washington Philosophical Society (1872). The specimens, which repre-
sent three very fine species of Paleopteris^ a Lepidodendrany a Siigmaria^
and a Carpolithes, were obtained from Lewis's tunnel, Alleghany Connty,
Virginia, in the lower part of the Sub-Carboniferons measures, near its
junction with the Upper Devonian.
Until recently there was, between these species of plants of the Cats-
kill and those of the Carboniferous type, a break of relation which
could not be accounted for, except by th^ supposition of a chahge of
formation, as it has been generally done for interruptions of this kind.
Therefore, the reference of the Catskill beds to the Devonian was judi-
cious so far ; but, two or three years ago, Prof. E. B. Andrew, while
connected with the geological survey of Ohio, discovered, in Perry
Connty, in the southern part of this State, a bed of black shale, with
abundant, well-preserved remains of ferns of peculiar and remarkable
type. These shale, from the remarks of Professor Andrew, are at a dis-
tance above the Chester limestone, or on the upper part of the so-called
Sub-Carboniferous measures of the West. Somewhat later, Mr. I. H.
Southwell, of Port Byron, Illinois, sent from that locality, as discovered,
also, in a bed of soil black shale, underlying the true Carboniferous
measures, a number of specimens representing some of the most pre-
dominant forms observed in the shale of Perry County. This pecu-
liar group of plants has still two species of Paleopteris, one of them
closely allied to P. Jachsoni, the other, like P. obtusa^ figured in Dana's
Manual of Geology, with some of the pinnules deeply emarginate at
the top, or bilobed. The majority of its species, however, are referred
to JUegalapteriSj a new genus established by Dawson, and represented
by ferns with immense fronds, large decurring leaflets, often divided in
the middle, in two lobes, by the forking of the middle nerve. One species,
of about the same character, is described by Professor Andrew* under
the generic name of OrUiogoniopteris. The specimens from Port Byron,
111., represent, also, more generally, species of MegalcptetiSj one of them
especially remarkable by the agglomeration or tufting of the terminal
leaflets, which divide, above the base, in two, more rarely three, equal
lobes, by the forking of the middle nerve, as remarked above. This
mode of division of the leaflets is exceptional in ferns of this kind, and
has never been observed except in one species of the lowest coal-bed oi
Illinois, the first above the millstone grit, and described in the 4th volume
of the Geological Beports of that State as Keuropteris /osciculataA
Professor Schimi)er, in his Vegetable Paleontology, mentions this
species as a very singular one ; and the discovery, in a lower member of
the Carboniferous, of species to which this peculiar conformation is trace-
able, afl'ords a point of comparison which cannot be overlooked in search-
ing either for geological relation or for an affinity of vegetable types.
Allied to the plants of the Catskill group by its PcUeopteriSj to the so-
called Upper Devonian of Canada by the Megalopteris^ the flora of Port
Byron pusses to that of the subconglomerate Carboniferous of Arkan-
sas by a small Arterophyllites, A. gracilis^ which is present, also, in the
shales of Perry County, and described, too, in the PreCarboniferous
flora ot Canada as A. parvula ; by Lepidodendron modulatum and L. car-
inatunij two species found also in Arkansas in subconglomerate coal-
beds; by Cardiocarpon Southwelliiy similar to C. ingens^ of Arkansas;
and it has, also, one species, Sagenaria depressa^ Gopp. of the Culm
or Sub-Carboniferous of Europe, and another intimately allied to
* Journal Science and Arts, December, 1875, pp. 462^-466.
t P. 3H1, PI. V, Figs. 1-4.
280 GfiOLOOICAL SUBVEY OF THE TERRITORIES.
Sphenopteris crassaj described by the same aaUior from tbe same forma-
tion, the Fosidonien schieffer. The examination of a large collection of
specimens from the coal-measures of Alabama affords the means of
pursuing the comparison of these floras somewhat further, for, till now,
the subconglomerate coal flora was merely known by the species de-
scribed from Arkansas.* That of Alabama is composed of a large
number of species as yet unobserved in this country; some of them,
however, described by European authors,- by Brougniart, Lindley, and
Button, especially, from the lowest coal-beds of England and of Ger-
many, inferior in station to the millstone grit.
There is, forexample, Spltem^pteris Hoeninghauaii^ predominant by a&
immense number of specimens ; three species of IJremopteris a coarae-
veined NeuropteriSy recalling the type of Paleopteris of tiie Old Bed;
many Lepidodendron^ some identical with species of the measures above
the conglomerate ; some of a peculiar type, one especially, with branches
covered both by leaves and scales, and Ulodendron minusj of the Lower
Carboniferous of England. Hence we have in the subconglomerate
coal of Arkansas and of Alabama another intermediate flora uniting
types of the coal above the millstone grit with those of the Perry shales,
as these serve as point of transition between the Gatskill flora and that
of the subconglomerate coal. It is thus to this point an uninterrupted
series of vegetable forms.t
The characters of the floras of both stages of the Carboniferous over
lying the conglomerate are well known. The lower, in connection witl
beds of coal of remarkable thickness, especially in the anthracite fields
of Pennsylvania, has a profusion of Lycopodiaceous. There abound
species of Lepidodendron^ Ulodendron^ Knorria^ genera represented
mostly by very large trees ; some ribbed Sigillarixj large-leafed species
of Alethopterisj of a type probably derived of the Megalopteris of old, like
A, Serliij A. iSuUwantii^ A. penrutylvanicaj A. lonchitioo^ with its numerous
varieties, A. nervosa^ which, like the former, appears already in nume^
ous specimens in the flora of the Alabama coal : SplietwpteriSj species
also related by their character to those of Arkansas, like S. Gravenhar%tii^
S. decipiens; numerous species of Hymetwphyllites^ and hard fruits, Car-
politheSj Gardiocarpi^ and Trigonocarpi, All this gives to the supra-coD-
glomerate coal a character which is especially predominant In the low-
est beds. In passing up to the Pittsburgh division, or to the upper
coal-measures, the constituents of the flora are gradually modified by
the decreasing number of the great lycopodiaceous species, which are
rarely found above the Mahoning sandstone of Pennsylvania, and by a
proportionate increase of the SigiUariw si>ecies, especially of the ecostate
section. We have in these upper coal-measures, besides these SigUlor
rtcBj a preponderance of ternsj arborescent species of FecopteriSj whose
large fronds and pinuse are spread upon the shale like small trees;
Fecopteris arhorescens^ P. unita ; some bushy Neurapteridece ; NeuropUrii
Loschii^ especially the most common of all ; a profusion of CalamiteM and
CordaiteSj and still one species of Aleihopteris^ A. aquilinaj a diminutive
form. Whenever remains of fossil plants are found in connection with
a coal, paleontology easily recognizes their relation to the upper or to
the lower division of the supra-conglomerate Carboniferous measures.
From this it follows that from the base of the Catskill group to that of
* Geological Report of Arkansas, vol. ii, pp. 295-;$l9.
t Prof. E. T. Cox, State fi^eolog^st of Illinois, has qaite recently sent me for determinatlos
a box of specimeDs from the' whetstone grit, 25 feet lower than the base of the confflomeiato-
They represent species either identical with or intimately allied to those of the flora of the
subconglomerate coal of Alabama.
UMQUEEKux.] EVIDENCE OF AGE OP LIGNITIC GROUP. 281
the Fermian, vegetable paleontology is able to discern and expose the
characters of five divisions of the Carboniferous, each determined by
peculiar species of plants, and each also relat.ed by analogous or even
identical species to both the preceding and the following stages of the
formation.
The records of the paleontology of the Coal-Measures are not less pos-
itively referable and less interesting to geology when they bear upon
questions, of a' wider and more general application. To my knowledge
no fossil plants from the Coal-Measures of North America were described
before 1818 ; in that year Eev. Steinhauer published in the Transactions of
the American Philosophical Society* his Fossil reliquiae where he de-
scribes and figures, under the generic name of PhitolithuSj a few species
of Calamites^ Lepidodendrony Vlodendron^ Artisia^ SUgmaria-y and Sig-
illaria. He mentions, however, in the introduction, that most of the
specimens of fossil plants from the Carboniferous represent ^i^icea (ferns).
After him Granger, in 1820, merely mentions a few specimens of coal
plants from Zanesville, and refers them to Steinhauer, species.t • From
that time to 1828, Granger, Cist, and Professor Silliman sent some spec-
imens of fossil plants from the Coal Measures of Pennsylvania and Ohio,
to Bronguiart, who was then preparing the materials for his greatcoat
flora. They represented, as seen from this work, ten species, three of
which only were then peculiar to this continent. In 1837, Dr. Hil-
dreth, of Marietta, so well known by his love and zeal for the study of
natural history, and its original researches in some of its branches, de-
scribed in the journal of his geological explorationsi a number of species
whose figures are mostly unrecognizable, and whose references are equally
nncertain. The remarks of the author, however, denote long and serious
researches into the distribution of the coal-beds and the fossil plants
recognized in their connection. For ten years after this nothing is said
upon our Carboniferous flora until 1847, when Teschermacher prepared,
on the fossil vegetation of North America, a very interesting and valu-
able, though too short memoir, published in the Boston Journal of Nat-
ural Hlstory.§ At that time the great paleontological works of Brong-
niart, Sternberg, Goppert,and Unger were already published, and there-
fore the author was able to more clearly analyze and describe the speci-
mens which, then, very rare, as he says, were obtained from New Scotia^
Bhode Island, and Mansfield, Mass. He is the first to remark upon
the affinity of the Carboniferous flora of America to that of Europe,
thus opening the way for a greatly-needed comparison between the
coal floras of both continents, to which some questions of high ijiterest to
geology were then and are still related. Teschermacher mentions in his
pamphlet twenty-three species, some of them described and obscurely
fibred also, all more or less positively referred to species known from
European authors except one. This, he says, has no relation to any
known by him. It is left without description and without name. The
flgare represents a fragmentary specimen of the most beautiful fern of
the Coal-Measures, Odontopteres Ayassizii^ which has never been found
bat in Rhode Island, and of which splendid specimens are preserved in
the Agassiz museum of Cambridge.
In 1850, Prof. H. D. Rogers, then director of the geological survey
of Pennsylvania, requested the assistance of a paleontologist for the
collection and the study of the fossil plants of the anthracite basin.
|_ ' - ■ ■ - - ■ ■ -.._■-.- . ^ 1 Jl L ■■■■■
* Vol. 1, new series, p. 265.
t Silliman^s Amerioan Jour. Sci., vol. iii.
X Ibid., Jaunarv, 1836, and Janttary, 1837, toIs. xxix and xzzi.
( Vol. y, part 3, June, 1847.
282 GEOLOGICAL SURVEY OP THE TERRITORIES.
The work was systematically begun and pursued, first, by tbe collection
and tbe examination of specimens of fossil plants in tbe difiereot coal-
strata of the anthracite, where, in some cases, coal-beds, exposed in a
vertical position and therefore disconnected, were .identified by their
vegetable remains only. The researches wei'e then extended for com-
parison in different parts of the so-called Appalachian or bituminous-coal
fields of Pennsylvania, in order to ascertain if both basins, that of the
authracite and that of the bituminous coal, were positively of a same
formation, and if the distribution of the fossil plants could indicate
not only identity of period, but conformity in the deposits of the coal-
beds. These questions have been examined and answered in the intro-
duction to the fossil flora of the coal-measures in the final Report of the
Geological State Survey of Pennsylvania, and the data which were ex-
posed by these researches have been accepted as reliable and recog-
nized ever since. This is followed in the same introduction by the com-
parison of the Carboniferous flora of Europe with that of Korth America,
as far $is this flora was then known, by more than one hundred species
described and figured in the Pennsylvania geological report, and by
as many more published in a catalogue of the fossil plants of the Ooal-
Measures, by the Pottsville Scientific Association in 1858, and reprinted
in Professor Rogers's report. The intimate relation of the coal floras of
both continents is there discussed and forcibly established by the ex-
position of identity of types, even specific identity for the greatest
number of coal-plants.
Later, vegetable paleontology was called to supply some evidence in
regard to the kind and degree of relation existing between the distribu-
tion of the measures of the so-called Appalachian coal-basin with those
of the Indiana and Illinois coal-fields, to which belongs the western coal-
basin of Kentucky. Researches of the same kind were pursued by the
exploration of coal-beds and the determination of the specimens of fossil
plants found in connection with them. The results of this study have
been published long time ago in the geological reports of Kentucky, un-
der the direction of Dr. Dale Owen, and in those of Illinois, under that
of Prof. A. H. Worthen. They have exposed, not merely a general
relation of the coal-plants of the western basins to those of the east,
bnt in most cases an identity of species, varied only by the presence
of a number of rare, peculiar forms, remarked once only atasole locality,
or seen again here and there, even at far distant points. This fact is
in accordance to the laws of geographical distribution, and repeated at
the difi'erent geological epochs as well as at this present time. Tbese
researches have proved also the intimate relation of the coal-strata in
regard to their vertical distribution in both the eastern and western
coal-fields, and therefore the synchronism of some of the moreimportant
coal beds over the whole extent of the North American Carboniferous
formations. Even then, from the harmony of distribution of the coal-strata
on both the eastern sides of the Indiana and Kentucky basin and tbe
western side of the Ohio Goal-Measures, as also from the identity of the
characters of their constituent plants, it had been inferred that the up-
heaval of the Silurian ridge which separates them has succeeded tbe
formation of the coal, and that therefore these now separated coal-fields
have been originally united. This opinion has been contested on con-
siderations derived from stratigraphical evidence. I think, however,
that new discoveries, like that of strata of exactly the same composition,
with plants of identical species, as the Sub-Carboniferous fossil-bearing
beds of Perry County, Ohio, and of Port Byron, Illinois, will corrobo-
rate the conclusions dictated by vegetable paleontology. Anyhow,
LE8QUEBEUX] EVIDENCE OP AGE OF LIGNITIC GROUP. 283
these researches have demonstrated thepossibleidentiflcation of the coal-
strata, a fact whose application, however, can become valnable to coal-
mining when we have more positive knowledge on the geographical and
stratigraphical distribation of the plants of the American Coal-Meas-
ures.
In the Permian, as far at least as this formation is known by the ex-
posare of its rocks in Iowa, Nebraska, and Kansas, near the janction of
the Platte witb the Missonri River, the records of vegetable paleontology
are blank indeed ; for the sufficient reason that this formation is repre-
sented there only by magnesian limestone or marine rocks whose only
fossil remains are invertebrate animals, the so-called Permo-Garbonife-
rous species, most of tbem indifferently referable to Carboniferoas or to
Permian. But sandstone rocks have been observed in the Ilocky Mount-
ains, which, without any animal remains, have been, from the nature of
their composition and from their snperposition to old Palt'ozoic strata,
considered as referable either to the Carboniferous or to the Per-
mian. A few fragments of Calamites only, found in connection with
this formation and sent for determination, were sufficient to estab-
lish its relation to the Permian, for the Calamites represented by these
specimens, G, gigasj is a leading plant of the Lower Permian. This case
was recently repeated from a locality far distant from the former, and
the same reference equally established from a few specimens only. It
cannot be said in this case, as for the Carboniferous, that the general
characters of the plants are well known, and that tiierefore vegetable
remains of this formation may he used sometimes for determination^ when
topography and animal paleontology cannot be taken, as guides; for, to my
knowledge, the above-mentioned specimens are tbe first vegetable re-
mains discovered as yet from American Permian rocks.
For the Trias, the evidence supplied by vegetable paleontology is pre-
sented in opposition to that derived from animal remains, by one of tbe
highest geological authorities of this country. This formation, exposed
in North Carolina, and in Virginia near Richmond, also, has important
deposits of coal, whose age has been for a long time in discussion among
geologists, and has been definitively fixed by tbe remains of fossil plants
found in connection witb tbem. In the last work published by Emmons,
American Geology, Part VI, tbe lower part of tbe section of page 17,
headed Permian, is described as tbe Chatam series, and its fossils, a few
fucoidal remains of uncertain affinity and a large number of animal re-
mains, crustacean, mollnskH, fishes, sanrians, are not considered as suffi-
cient to authorize adecisiou upon the age of tbe format ion, which is there-
fore left as uncert in. The upper part of the measure, however, has in
its divisions layers of shales, wi"h plants, and though remains of animals
are not found in connection with this series, it is positively determined
as Triassic by tbe author, from vegetable paleontological evidence
only. Tbe characters of tbe plants, as indicated especially by the
CycadecB^ relate this flora to tbe Jurassic of Europe; hence it^s appella-
tion ot Triasso- Jurassic, given to tbe formation. I say the Jurassic of
Europe, for indeed this foi*mation is as yet so indefinite in this country
that it has no records of any kind which may be used as points of com-
parison. Its flora is totally unknown ; and even if we had a few vegeta-
ble remains obtained from tbe strata considered as Jurassic in the Black
Hills, the Uinta Mountains and the Sierra Nevada, it is very questiou-
ab!e if they could be used for identification of tbe formation. The Ju-
rassic, even for Europe, is the dark age of vegetable paleontology. Ex-
cept the oolitic coal deposits of £nglan<l, its strata of enormous thickness
284 GEOLOGICAL SURVEY OF THE TEBBITOBIES.
in some regions are mostly marine, and have as 3*et afforded too scantr
materials to define somewhat clearly the characters of its flora in the
numerous subdivisions of the formation.
The Cretaceous flora of Korth America, as far as it is known from its
representatives in Kansas, Nebraska, Dakota, and Minnesota, has beea
reviewed in this report and speaks for itself. Its characters, as they
are known now, will be more expressively compared to those of the
Lignitic flora, and the differences more distinctly seen when the Tertiary
species are published with fignres. From the multiplicity of its types,
some of them transient or indefinite, it is now easily understood that
the attempt of a comparison of the few first leaves discovered in Ne-
braska could but mislead the most competent and careful paleontologist
in looking for typical relation in order to determine their age. The
recordsof this Cretaceous floracould not be read, indeed, before they had
been written, or when they were exposed by a few scattered words only.
Now the North American Cretaceous plants represent a definite group,
which, though susceptible of wide extension by new discoveries, has its
essential characters already defined, and is thus available as a point of
comparison for paleontological documents, either from this country or
from Europe. It is in this point of view especially that the importance
of the publication of the fossil plants of this country has to be judged.
That the geological age of the Dakota group flora, as long as its char-
acters were unknown, should have been subjecti^<^ to the evidence af-
forded by its overlying marine strata, which wert> clearly determined
by invertebrate animal remains, is a matter of course. But now this
flora affords a collateral evidence which by its vegetable types may be
used for geological determinations just as legitimately as the fauna.
From a subordinate it becomes an assistant.
I consider that this discussion upon the authority of vegetable paleon-
tology in regard to the determination of the age of the disputed strata,
Cretaceous Lignitic or Lignitic Tertiary, has been of great value to Amer-
ican geological science. It has induced wide and more careful researches,
and brought forth a large number of important discoveries which, with-
out it^ would have probably been indefinitely postponed. No depart-
ment of geology should be disregarded or considered as of an inferior
concern. All have an equal right as members of^a same body. And
was it only for the reason that vegetable paleontology has been gen-
erally, and is still now, considered by many as of little value as an as-
sistant to geological pursuits, I am the more disposed to |)ersist io
putting it forward as an authonty superior to that of animal pale-
ontology for the determination of the age of the strata of land forma-
tions.
The above remarks all tend to the same purpose, and serve as an in-
troduction to a more detailed examination of the age of the Lignitic as
exposed by the fossil flora.
To appropriately enter into the subject, we should have a clear under-
standing of the now adopted names and limits of the numeroussubdivis-
ions or groups of the Tertiary, as marked by European authors. Though
it may be that some of these groups are not positively defined, either ia
their geological relation or in their paleontological characters, they are
serviceable for comparison.
Table of subdivmons of the Tertiary of Europe^ axjcording to the floras.
Pliocene. Lower limits not positively fixed: Uirgely developed in
Italy.
Paleocene.
Vw
i.x8QUBR£ux.1 EVIDENCE OP AGE OP LIONITIC GROUP. 285
c OeniDgen.*
Miocene. < Mayeociau or Helvetian.t
( Aqaitaniau.j:
ArmissaD, Bonnieax, aud Manosque, France, intermediate between
the Lower Miocene and the Oligocene.
Oligocene. Tongrian. §
i?^vn<ina ) Gypses of Aix, Alam Bay, Monnt Bolca. London Clay.
jLocene. ^ Sheppcy, Ores of the Sarthe.
I ' Upper Landenian : Sezanne same as the Belgian Panise-
lian.
Lower Landenian : Sand ol Brachenx, Lignitic soisson-
-{ nais, (Snessonian.)
nersian: Gelinden.
Limestone of Mens, unconformable to the Cretaceons of
Maestriehy which it overlies.
' Some authors consider as Cretaceous the sands of Bracbenx and Gel-
inileD, as indicated by the characters of the floraof Gelinden.
These subdivisions of the Tertiary of Europe seem to expose a pro-
digious thickness of the formation, and to indicate a great dispropor-
tion of vertical extent in comparison to the American measures of the
same age. There may be indeed a marked difference but as vet very
little is known of the Tertiary of this continent, and certainly this little
takes already, by its wide area and the thickness of some of its divis-
ions, an important place in the North American geology.
Last year Prof. F. Y. Hayden discovered, near Point of Bocks,
some beds of shale with rich deposits of vegetable remains, and obtained
a large number of specimens. This locality is between Black Butte
Station, nine miles northwest of it, and Salt Wells, another station of the
Union Pacific Railroad, about the same distance farther west. From
Prof. B. F. Meek's report and from my own || it may be seen that from
Black Butte to Point of Bocks, in following the railroad, the northeast-
ern dip of the measures brings successively in view a series of heavy
sandstones, interstratified with beds of clay and lignite, whose whole
thickness, according to Messrs. Meek and Bannister, is estimated at
about 4,000 feet. The series of these rocks is beautifully exposed by a
diagram in the report. My own esti mation gives only half this thickness.
But as I did not take any measurements, the purpose of my explorations
'Represented at Lode, MontAroD, AlbiSf Steckborn, 'E\gg (Switzerland); Schossnitz
(Sileiiia) ; Gnusburg (Bavaria) ; Parscblug and Gleichenberg (Syria) ; Tokay (Hungary) ;
Singaiplia, Stradella, Guarene, Sarzanello, Val d Arno (Italy).
t Represented at Delmont, Deveiller, Aarwang, tunnel of Lausanne, Calvaire, Riant
Mount, 8t. Gall, Solitude, Mbnglen, Ruppen, Alstiitten, Oberaegeri. Buron (as Mayen-
cian) ; at Petitmont, Estave, Croisettes, MontenatUes, Moudon, Payorne (as Helvetian),
(Switzerland); Bovey-Tracy (England); Monte Bamboli, Snperga (Italy); Menat, Ger-
aovia (France) ; Le Khon, Wetteren (Lower Ligoitic), Basin of Mayence, Kempter, Gnnz*
burg (Germany) ; Bilin (Bohemia) ; Radoboy (Croatia) ; Tohnsdorf, Koflacb, Eibiswald
(Styria) ; Basin of Vienna (Austria).
t Represented at Railing, Scbwartzacbtobel, Waggis, Vevay, Monod, Rivaz, Dezaley,
Paudez, Rochette, Conversion, Bruits, Rufiberg, Bossberg, Udhe>Rhone (Switzerland);
Specbbach (Alsace); Lower Succinifer Tertiary of the Baltic, Spitzberg, Iceland, includ-
ing, perhaps, the whole miocone series, Greenland, Mackenzie, Alaska; Cardibone, Selzedo,
Novate, Zorencedo Vegrone (Xtaly); Kumi, liiodroma (Greece); Menat (France); Rot,
near Bonne, on the Rhine.
$ Armissant Peyrac, Saint Jean of Gargnier, Basin of Marseilles, St. Raccharie (Var.),
Aptf Gypses of Gargas, Vauduse, Castellane (France) ; Sechbach and Lobsart (Als'^ce);
Mount rromine (Dalmatia); Sagos (Krain) ; Haering (Tirol); Sotzka (Styria); Peissenburg
and Miesbach (Bavaria); Alsattal and Kushlin (Bohemia); Sieblos (Khun Mountains);
Beemstadt and Wtlssenfiold (Thnuuppa). . These data on the distribution of the
Tertiary in Europe are moetly derived from Schimper's Vegetable Paleontology.
I Dr. F. V. Haydeu's Sixth Annual Report for 1872. Professor Meek*s sections and dia*
gram of the measures are given at pp. 530, 539, 534.
286
GEOLOGICAL SUBYEY OF THE TERSTTOBIES.
in that part of the country being especially the research and stody of
vegetable remains, I readily admit the conclusions of these distingnis^^ied
geologists who had time to attend to details of stratigraphy. As Poiot
of Eocks Station, where the specimens of Dr. Hayden were fouud, is al
a distance of a few miles from the cat end of the ridge east of Salt
Wells, the thickness of the measures is there somewhat less, say about
three thousand feet. Though it may be, such a heavy series of strata is
passed from Black Butte to Point of Rocks that if any part of the so-
called Bitter Oreek seiies is Cretaceous, we may expect to find in the
fossil plants of this last locality a number of species of Cretaceous tjjies,
or at least a distinct modification in the characters of the plants. The
thirty species represented by the specimens of Point of Eocks are de-
scribed hereafter, but the deductions derivable from the determiDation
of these plants in regard to evidence of geological age, will be more clear-
ly understood by a comparative table exposing affinity or identity of
characters with species of other localities. The points of comparison
are indicated with the flora of the European and of the Arctic Miocene,
of the Canadian Tertiary, of the European Eocene, of Golden, Black
Butte, and of the Cretaceous in general.
Table exposing the relation of the fossil-plants of Point of Rocks,
Species of foaail-plonts Aroin Point of Rockji.
m
1
§
a
«
i
■
1
s
s
1
<
»
••
a
s
i
•
a
«
1
5
&
t
Cretaceooa.
1. Pncas limltnm...................... ...........
An.*
An.
An.
8. Salvioia attonnata
3. Selaffinolla falcata
An.
An.
4. Selaffinella lacioiata
"id."
"id.
■■■"■■
5. Seanoia breTifolia
"ii
6. Seaaoia lonsifoiia
An.
7. Scanoia biforniis
Aa.
8. WiddriDirtoDia comDlaoata
An.
ft. Pintia cormimta r, ^ -r--
Id.?
Id. !
Ab.
10. LemDa acntata .............................
11. Ottella Ammicana - ,^.,^,-.^ ^^^
12. Sabal irravana
An.
An.
An.
Id.
Id.
VancoaTer. .
13. DrvoDnvllnm sobfaleatam ......................
14. Drvoob vllum creuatom ........................
15l PoDnlmi malanaria ....... .. ..
Id.
Ifl- PnnnlnR mAlftiiRmldAA
An.
17. Fleas amrifolla
Id.
Id.
18. Ficcm dalmatica ............. ..... ...
19. Fleas Dlanicoetata j.
An.
"ii"
Id.
Id.
Id.
90. Picas tUlsfolia
Id.
2 1 . Ficns irreffalarifl ....
22. Traoa microDbylla
.An.
23. liftflniff proRStaRif
An.
24. Vibomam rotandifollam ......................
An.
Id.
Id.
Id.
23. Vibomam WhyiDDeri
Id.
26. Vibaraam manrinatam
An.
*"ii'
27. DioroTroa bracbvaeoala
Id.
28. OrevioDSls Clebaml
An
2ft. RhoH mnmhrannAAA ..
An.
30- Ino-lAna rhomnoidM ..,
Id.
....
*Aii. for analagoua ; Id. for identi^l.
Of the thirty species enumerated in this table, one is identical with
a Canadian species recognized as Tertiary, as seen below, from quota-
tions of Prof. G. M. Dawson's Geological Report. Six are identical with
and six also analogous to those of the Lower European Miocene, two are
identical with, and one allied to, Arctic Miocene species. Six have a
close relation to those of the Lower European Eocene, or rather of the
UE8QUKBXUX.] EVIDENCE OF AGE OP LIGNITIC GKOliP. 287
Tertiary divisioD, separated at its base under the Dame of Paleocene.
Three are identified and two analogous, in the flora of Oolden. Nine
identical and one analogous, in that of Black Butte ; and four have an-
alogy with Cretaceous forms.
The relation of Point of Bocks with the Canadian Tertiary is especially
niarkecL by Lemna soutata^ a floating plant, described by Prof. J. W.
Dawson, in the report of the geology and resources of the region in the
Ticinity of the forty-ninth parallel. The geologist of the commission,
Prof. George Mercer Dawson, obtained the specimens from a bed of clay
near the very base of the Lignitic formation, where, according to the in-
formation kindly furnished to me, the vegetable remains representing
this species were very abundant, but difficult to get from the crumbling
shale. Though their reference to any living species is not distinctly
marked, the peculiar character of the plants does not permit any doubt
aboat its identity with that of Point of Bocks, which is also represented
by numerous specimens. Half the specimens from this place bear re-
mains of this species and of another, Pistia corrugata^ which may be a
mere form of the same. In regard to the identity of the Lignitic meas-
ures of Canada with those of the United States, the evidence is equally
conclusive. The report quoted above proves it, by good sections and
diagrams, which indicate the same distribution of Lignitic beds, clay,
and sandstone strata, as in the great Lignitic of the Bocky Mountains,
of which that of Canada is a mere continuation. It enumerates, also,
besides those which are descirbed, a number of plants from the Lower
Tertiary, of a higher stage, mostly of Miocene types.
In remarking upon the fossil plants which he had to determine, the
celebrated professor of Montreal, J. W. Dawson, says, ^^ That the plants
of the first group are for the most part identical with those found by
American geologists, in the Fort Union series, and which have been de-
termined by Professor Newberry and by M. Lesquereux. They are
also similar to plants collected by Dr. Bichardson, in the Lignitic series
of the Mackenzie Biver, as described by Heer, and represented by speci-
mens in the collection of the geological survey, &c. They also approach
very closely the so-called Miocene floras of Alaska and Greenland, as
described by Heer, and in their facies, and in several of their species,
they coincide with the Miocene floras of Europe.'' He then adds, <^ If
we were to regard the affinities of the plants merely, and to compare them
with the Miocene of other countries, and also to consider the fact that
several of the species are identical with those still living, and that the
whole facies of the flora coincides with that of modern temperate Amer-
ica, little hesitation would be felt in assigning the formation in which
they occur to the Miocene period. On the other hand, when we consider
the fact that the lower t>ed3 of this formation hold the remains of rep-
tiles of Mesozoic types ; that the beds pass downward into rocks hold-
ing Baculites and Inocerami; and that a flora essentially similar is found
associated with Cretaceous animal-remains, both in Dakota* and Yan-
couvei^s Island, we should be inclined to assign them at least to the base
of the Eocene.
From this it seems that Professor Dawson does not separate the two
essential groups of the Tertiary: the upper one with its Miocene types, a
flora indicating a temperate climate like that of the middle zone of the
United States ) the lower one with its numerous species of Palms, of Ficus,
&c., evidently representing a subtropical vegetation. In this last flora,
the one which is now under examination in this paper, there is no
species identical or analogous to any of those of the Dakota group.
* The assertion is right for Yancouver^s Island bat not for the Dakota group.
288 GEOLOGICAL SURVEY OF THE TERRITORIES.
The extraordinary separation of both floras has been safiQciently estab-
lished by former comparison and descriptions of species. In the apper
stage some rare typnes of the Gretaceoas re-appear. Bat appareotlj
the specimens obtained by the survey mostly represented the upper
stage of the Canadian Lignitic. For Professor Dawson describes and
enumerates, from Porcupine Greek, seventeen species, all of Miocene
type, and most of them formerly described by Professor Heer and
Professor Newberry, from the Miocene formations of Alaska, Greenland,
and especially from the Union group, with which the Poicnpine Greek
group appears closely allied. These plants are:
Equisetum species, similar to E. arcticum Heer.
Glyptostrobus Europeus, Heer.
Sequoia Langsdorfii Brgt.
Thuia interrupta Newby.
Phragmites t species.
Scirpns species.
Populus Bichardsoni Heer.
Gorylus'rostrata Ait.
Gorylus American. Walta.
Diospyros species.
Bhamnus concinnus, Newby.
Gary a antiquorum, Kewby.
Juglans cinereaf or J. bilinica, Ung.
Viburnum pubescens, Pursh.
To this and by comparison are added the species catalogued by Heer,
from Bichardson's collection on the Mackenzie, which| says Professor
Dawson, belongs to the same region. They are :
1. Glyptostrobus Europseus Heer.
2. Sequoia Langsdorfii Brgt.
3. Piuus species.
4. Smilax Franklini.
5. Populus Bichardsoni.
6. Populus arctica.
7. Populus Hookeri.
8. Salix Bheana.
9. Betula species.
10. Gorylus Macquarrii.
11. Quercus Olafseni.
12. Platan us aceroides.
13. Hedera McGlurii.
14. Pterospermites dentatns.
15. Phyllites aroideus.
16. Antholithes amissus.
17. Garpolithes seminulum.
The species described in the same report from the lower stage of the
Lignitic of Gauada are fewer and apparently represented by more im-
perfect specimens. They are Equisetum Parlatoriij Heer, of the Miocene
of Europe, a species to which U. Haydenii of Garbon is closely allied.
Its habitat is marked as Great Valley.
Lemna scutata sp. nov., abundant at the Bad Lands, and also at Point
of Bocks.
Scirpus species. Bad Lands.
Salix Ehetma f Heer (Great Valley), species of the Miocene of Green-
land.
L«fiQUEiiEcx.j EVIDENCE OP AGE OP LIGNITIC GROUP. 289
Sapindus affiniSj Newby, (Bad Lands), species of the TTuion groui^.
Jthamtimy an undescribed species (Great Valley), corresponding, by
its preserved part, to R. Eridani Ung., which is Ficus jynXj a Miocene
species of Europe and of the upper American Lignitic also.
Aescultis antiquusj Trapa horealis^ and CarpoUthes^ three new species,
described from obscure specimens, from the same locality as that of
Lemna, the Bad Lands, west of Woody Mountain.
From the exposition of this flora, it is not surprising that Professor
Dawson should admit, as the result of his study of the fossil plants of
the Lignitic, the Tertiary age of these formations. For, indeed, in this
flora there is, as remarked already, no trace of any vegetable remains
which, by comparison with the species of the Dakota group or with
those of the Cretaceous of Europe, could be recognized as identical or
even related to any of them.
Coming back to the other plants of Point of Bocks for considering
their characters for an evidence of their age, by comparison with other
groups of floras than that of Canada, we find in the table three of them
marked as analogous to Cretaceous types. The first, Pistia corrugataj
may be, as remarked in the description, an undeveloped or young form
of Lemna scutata^ a question here without importance. At first I con-
sidered this species as being the first of this genus recognized in a fossil
state, for none has been published as yet. But Count Saporta informs
me that a species, Pistia Mayelii, Sap. ined., has been found in the fresh-
water Upper Cretaceous of Fuveau, France. From the sketch kindly
communicated by the author, his species appears very different in its
characters from that of Point of Bocks. The generic affinity, however,
is worth remarking, for a plant so profusely represented as is our species,
which, by itself or mixed with. Lemna scutataj covers both sides of a
number of large specimens.
By the same degree of affinity, I have marked in the Cretaceous col-
umn of the table Sequoia longifoliaj also found at Black Butte, and
Sequoia biformis; the first on account of a distant likeness to S. Smit-
hiana, and the other to S. ReicJienba^shi and 8. rigida, three species
recognized, the first in the lower, the two others in both the upper
and lower stages of the Cretaceous of Greenland. The wide distribution
of Sequoia species is generally known ; it is marked here by the presence
of these two species in two stages of the Cretaceous. But without
taking into account the longevity of these forms, we have to consider
that if we have here two conifers merely related to Cretaceous species,
this cannot eliminate the testimony of Sequoia brevifolia, which is as
profusely represented in the flora of Point of Bocks as Pistia, and by
specimens in a perfect state of preservation. One-half of the specimens
of Mr. Cleburn, besides a large number of those of Professor Hayden, show
it in its two somewhat different forms. As it is distinctly and easily
determined, its characters being precise, and as this conifer is a repre-
sentative of the Miocene flora of Greenland and of that of the Baltic, its
documentary evidence is more positive than that of the two other Sequoia
represented as yfet by small fragments, and merely allied to Cretaceous
types.
I consider as referable to the Eocene by analogy of distribution Sabal
Orayana and the two species of Dryophyllum of l?oint of Bocks. That
Palms have originated in the Cretaceous is now an established fact.
Schimper, in his Vegetable Paleontology, Indicates as from Cretaceous
formations two species of uncertain affinity. And nevertheless, in a
more recent work, the Flora of Gelinden, by Saporta and Marion, the
authors remark that one species of Palms only was known by its fronds
19 n
290 GEOLOGICAL SURVEY OF THE TERKIT0BIE8.
from the Gretaceoas. The recent discovery by Schweinfarth of a frait,
Palmacites rimoamSj Heer, * in the Upi)er Oretaceoas white chalk of the
oasis of Chargeh, west of Thebes (aboat 25^^ latitude north), is another
evidence of the presence of palms in the Upper Gretaceons. That, bow-
ever, remains of this kind are extremely rare even at the end of the
Gretaceons is proved by the importance attached to the discovery of a
fruit of this kind in a region under the tropic. From the Paleocene, as
represented in the floras of Gelinden and of Sezane, no species of Palms
have been positively determined. For the fragments de-scribed in this
last flora under the generic name of Ludoviopsis are indefinitely referred
by the an thor either to the PandaneaB or to the Palms. As yet, of the fifty
species of known fossil Palms from their fronds, twenty belong to the Mio-
cene, especially to its lower stage ; eight are described from the Tertiary of
Italy, without reference to any of its divisions, nine are Oligocene, twelve
Eocene, and one Gretaceons. Of the eight species of Sabal described, one
species is Miocene, two Oligocene, and five Eocene. tSabal andegarfenm
Schp., and 8. precurgoria Schp., two species of the Upper Eocene of
France, are very closely related, the first to Sabal communis of Golden,
the other to 8abal Orayana found in many localities of the Lower Lignitic,
from Mississippi to Vancouver. In considering the Liguitic flora by the
specimens of fossil plants from Black Butte, Golden, Golorado Springs,
the Baton Mountains, &c., where the preponderance of remains of
Sabal and Flabellaria is so marked, how could it be i)0S8ible, if even we
had no other characters for direction, to refer it to the Gretaceous f The
above speaks plainly, and shows how I had to recognize the flora of
Vancouver as Tertiary, from the numerous specimens of Sabal sent by
Professor Evans from Nanaimo, even if the other plants of the locality
had not represented Tertiary types. It was the same case for the flora
of the Mississippi State, where the Palms are also in preponderance. At
Point of Bocks, four large specimens upon sandstone represent the same
species of Sabal as that of Vancouver and Mississippi, 8. Orayana^ which,
in the opinion of a celebrated European paleontologist, is one of the
finest and most positively characterized species of the genua
The two species of Dryophyllum described from Point of Bocks are
indicated in the table of distribution as analogous to the Eocene. This
genus represents a separate section of the oaks, corresponding by the
form of the leaves and the indentations of their borders to the Ghestont*
oaks of the present North American flora. Messrs. Debey and Etting-
hausen have separated it for the classification of some leaves found in the
Gretaceonsof Belgium. It represents, therefore, a Gretaceous type, which,
however, like some others of the same formation, FagnSj Platanfis^ &c.,
does not appear to have reached its full development from or at its origin.
We see it, for example, in the Dakota group flora, in the proportion of
two species in about one hundred and thirty, while in the Paleocene flora
of Gelinden it has four species in thirty, and the same number in forty-
eight in the flora of Sezane. It then re*appears by more or less numer-
ous representatives in analogous species of QuercuSj and may therefore
be followed nearly without interruption to the present time. From this
it is clear that the reference of fossil species of this genus, when
remarked in connection with remains of Tertiary plants, should more
appropriately pertain to the Eocene than to the Gretaceous. Therefore
if the presence of species of Dryophyllum in the Point of Bocks flora,
and that also of Pitsia^ Sequoia btformis^ and Sequoia longifoliOy im-
* Ueber foesile fnichte der Oase Clwrgeh, 0. Heer, in Denka. der Schweis, Katnrf.
Gesells., vol. zzvii, 1876.
LtsQUEHBux.] EVIDENCE OF AGE OP LIGNITIC GROUP. 291
prints to it an odd physiognomy, it is either as remnants of tbe past,
merely recording a few features of old generations passed awc'vy, or as
contemporaneous long persistent types, which do not distinctly charac-
terize any peculiar epoch. As proof of this assertion we have the true
Lower Eocene character marked in the same flora of Point of Eocks by
four species, Fictis planicostata^ Viburnum margiruitum^ Populus me-
landrioideSj and Oreviopsia Cleburniy which evidently, related to species
of the Sezane flora, though in various degrees, have no affinity what-
ever to Cretaceous types.
The flora of Point of Socks is related to that of Black Butte by nine
identical forms or by one-third of its species. In considering the evi-
dence of synchronism, the identity of two floras could not be more posi-
tively proved than this, and nevertheless we have here two to three thou-
sand feet of interposed measures. It is a remarkable fact, upon which
more will be remarked presently. The group of plants at Point of Eocks
has, besides the Eocene representiitives. six species identified with, and
as many related to those of the Miocene of Europe. Therefore wo see
here, what has been remarked in other localities of the Lignitic, a com*
pound or admixture of old and young tertiary types, in comparison at
least with the fossil floras of Europe, and thus a general character which
does not distinctly relate to any peculiar stage of European Tertiary.
We have the Paleocene by relation to species of Sezane ; the Upper
Eocene, especially the Ligurian or Oligocene, by the Palms, and the
Miocene by a number of common and generally distributed forms which,
like Sequoia langsdorfii^ Fopultu mutabiliSf Fious tilicefolia^ Cinnamomum
missisHpiensej Ehamnus rectinerviSj Juglans rugosaj &c., are omnipresent
and constant types, indicating merely the Tertiary age for the Lignitic flora.
For this reason I shallcontinue to carefully record its pointsof affinity with
the divers groups of the geological floras of Europe : but at the same
time denying as yet sufficient evidence of identity to any of them I
persist to consider it simply as the Lower Eocene flora of this continent.
I said above that the identity of specific forms at Point of Bocks and
Black Butte was worth recording more carefully, as a remarkable
case in regard to the distribution of plants. In marine strata the long
preservation of types is a matter of little concern, for the circumstance
under which the marine faunas are distributed may be the same for very
long periods, as, for example, the mineral elements entering into the com-
pounds, the depth and temperament of tbe water, &a But thatacompara-
tively large number of land or fresh-water plants, subject to modifica-
tions or forced to migrations by atmospheric changes, may be preserved
identical through the lapse of time indicated by the thickness of the
measures heaped along Bitter Greek, has not been proved by as positive
an evidence as we have it here. The distance between both localities is
eleven miles only, and the superposition of the strata is all along so
dear, that there is no possibility of any mistake in the calculation of the
vertical space sepaxating both points. It is scarcely possible to hazard
a corgecture upon the length of time indieated by the building up of
these intermediate measures. Evidently of a shore formation, the heap-
itt|C of their materials may have been more rapid than for the deposits
at the wide bottom of the sea. They evidence, however, in their suc-
cession, a series of sandstone beds which though of greater thickness
are interstratified by beds of clay, built up of swampy deposits of long
duration and especially of coal-beds, still more clearly denoting the slow
progress of the work.
A geological fact like the one remarked between the relation of the
floras of Point of Bocks and Black Butte and the positive evidence of t he
292 GEOLOGICAL SURVEY OP THE TERRITORIES.
long periods of time and formations whicli separate them is an instrnc-
live document, whose importance as point of comparison in the study of
the geographical distribution of our present flora and of its analogy to
ancient types will be easily accepted by botanists. But here it has to
be considered merely in connection with the question of the age of the
Lower Lignitic.
The Cretaceous Dakota group is separated from Point of Bocks by a
thickness of strata about the same as that which is marked between
Point of Eocks and Black Butte. Nevertheless, between the floras of
the Nebraska and Kansas Oretaceous and that of Point of Bocks and
Black Butte, we find scarcely any analogous type, and not a single
identical form. The erosions may have indeed considerably thinned
the marine strata representing the Cretaceous above the Dakota group,
but that cannot lessen the strength of the deduction made from the
total disconnection of two floras, one of which denotes by its essential
characters a marked dissimilarity of atmospheric circumstances, a
weighty evidence, if not a positive proof, of a change of epoch, if not in
the sea, at least upon the land. It is useless to repeat that, as yet, no
marine invertebrate remains of Cretaceous type have been discovered in
the whole Lignitic measures above Point of Bocks. We may admits
however, that while the Tertiary age was, at its beginning, represented
as a land formation, as seen by its flora, a Cretaceous marine fauna may
have still locally persisted in deep seas. Facts of this kind are recorded
in European geology. The presence of the Saurian Agathaumas in the
Lignite bed of Black Butte is then certainly explainable as denoting the
wandering of that animal out of its domain, and its death by i>enetra-
ting into a peat-bog and being irretrievably swallowed by its soft mat-
ter. If once imbedded in soft peat, no animal, not even man, can get oat
of it. By this fact, and also from the reason that the coriaceous, ligne-
ous plants of the bogs are not food for mammals, I explain the scarcity of
bones of Eocene animals in the lower beds of the Lignitic. As a shore
formation, a surface covered with deep bogs surrounded by sand wastes,
this primitive land would not aflbrd food to mammals or even be accessi-
ble to them. Every one who has explored a peat-bog knows how these
formations are deprived of animal life. Very few bones of the
Aurochs have been found in the bogs of North Germany, and the area
covered by the Lignitic shows how compact and continuous, not to say
universal, were those swamps of the Lower Tertiary. I l)elieve, there-
fore, that if the bones of Eocene mammals are not discovered in the
lowest part of the Lignitic, they will be found in the upper strata.
Moreover, the agglomeration of bones in certain localities depend on pecu-
liar circumstances, and donotimmediately and forcibly relate, like plants,
to the general characters of a whole period.
The question of the subdivision of the Lignitic or Tertiary measures,
which I have separated in four groups, from the non-coincidence in the
general character of the flora, is still disputed, and this division con-
tradicted by the assertion that the discordance is merely apparent,
and a result of the geographical distribution of species, as we may
see it now in groups of plants at distant localities. The contempo-
raneity of the fossil floras is not merely marked by the identity of some
species, but also by a kind of general character denoting the same
climatic circumstances. The modification due to the geographical dis-
tribution may be easily recognized by the presence or absence of a
number of species in the flora of the Bitter Creek basin, of that of
Colorado, the Baton Mountains, the Lower Union group, the Missis-
sippi, and Vancouver. There is between these localities a wide dis-
IXSQUEREUX.J EVIDENCE OF AGE OP LIGNITIC GROUP. 293
t£ince; and, indeed, tbe Yancoaver flora may show, in its details, marked
points of dissimilarity to that of the Mississippi. But, one of the prom-
inent characters of the Lower Lignitic is the predominance of Palms,
and we find it manifest in all the localities named above. Indeed, 1 have
found remains of Palm, espeoially of Sabal, whenever I have seen Lower
Liguite beds; and, as it has been remarked formerl^^, iSoZ^a^ Grayatia has
been observed on specimens from Vancouver, Point of Bocks, Golden, the
Mississippi, &c. With this there are, in all these floras, a predominance
of subtropical forms, and the absence of northern types, rendering more
evident their correlation iu time. Sufficient details have been given on
the species of the group, and on their distribution, in Dr. Hayden's
former report (1873), p. 378 to 390.
The group of plants of the Evanston division has, as yet, no remains
of palm -leaves, but fruits doubtfully referable to the Palm family;
with this it has some of its species of leaves represented at Golden,
others at Carbon. The general character of its flora does not indicate
as high an average degree of temi)erature as that of the Lower Lignitic.
The group has been separated, as an intermediate one whose relation is
not positively fixed now. According to Professor (3ope^s description,
bones of Eocene vertebrate animals have been found iu connection with
it. Its true horizon may be rendered more definite by further discoveries.
But in the group of Carbon the general character of the flora is evident,
and its relation to the Miocene of Europe and of Greenland is exposed,
not only by this general kind of related facies, but also by a number of
species, like Platunus aceroides and Ouillelmw^*. Acer^ Fopulus arcticaj
Taxodium dubiumy Alnus Kefersteinii Betula^ Quercvs^ CoryluSj indicating,
together with the total absence of Palms, a marked difl'erence in the
climatic circumstances governing the flora and that of the Lower
Lignitic group. This difference, also, is not remarked at Carbon only.
It is reproduced in the same degree, by general affinity and identity of
species, iu the flora 6f Coral-Hollow, San Joachin County, and of Con-
tra Costa, south of Mount Diablo, California ; of Bridge Creek, John
Day Valley, and of Blue Mountain, Oregon; of Bellingham Bay, of
Alaska, as established by Heer's flora of that country, and therefore fol-
lowed northward from Carbon to Greenland. Some of its types are so
definite that a single specimen of a species of Acer or P/dto^u^ would
suffice to positively identify this group as Miocene, just as a few spec-
imens of Quereusfurdner vis proved the Eocene age of the Cascade Mount-
ains of Oregon, whose formations were at first supposed to be Post-
Tertiary or of recent origin.
A few words more will be sufficient to answer the other objections
recorded at the beginning of this paper against the value of vegetable
paleontology in its application to geology for the determination of the
age of the formations. We know now well enough that remains of
fossil plants are abundantly found in the land deposits of this continent.
The result obtained from the onset of American researches in vegetable
paleontology let us surmise what an immense amount of documentary
data the after-coming geologist shall be able to gather in the same
field. The authority of animal-remains shall continue undoubted as far
as it refers to marine formations. But when land formations are to be
considered, theauthority should, when evident, be accepted as decisive.
* The fragment of leaf fonnd in connection with the bonee .of the Saurian at Black
Batte, and conaidered, from the character of nervation of the middle of Uie leaf, the only part
preserved, as doabtfnlly referable to P. GuUldnuB f was identified from better specimens,
showing the outlines of whole leaves, as a new species of VUfUimum, described in this paper as
Vibumun ptatanoides.
294 GEOLOGICAL SURVEY OF THE TERRITORIES.
There may be some exceptioDal cases where both kind of evidence may
be in opposition^ however, and afford reasons for dispute of anthority.
For example, no Cretaceous invertebrate marine remains have been fomid
in the strata of the Lignitic above Point of Eocks, nor in the Bitter
Creek series above this point, nor in the whole extent of the Colorado
Basin ; hence the plants, being characteristic and Tertiary, the whole
formation should be admitted as Tertiary, of course. But Vancouver
shows, as far as its flora is known, identity of characters of its fossil
plants with those of the Lower Lignitic, as known, from the above-named
stations ; its relation is therefore defined as land formation, and this
should be to my persnosion considered as evidence of synchronism and
therefore of its Tertiary age, though the beds bearing Tertiary plants
may be locally and casually overlaid by marine strata with Cretaceous
animal-remains. This case has some analogy with that of the presence
of the bones of a Cretaceous Saurian at Black Butte.
Conformability or uncomform ability of stratification proves very little
in regard to the changes which are considered as indicating a new epoch
or period. Of course the disturbances of wide-expanded surfaces of the
earth modify in various degrees the atmospheric circumstances, and, in
a less degree, however, those which govern the distribution of animals
under wat^r. Therefore the changes in the characters of the floras or
the faunas may be more or less evident in correlation with these dis-
turbances. But these are more generally so gradual that they cannot
be remarked by traces of unconformability, and the consequences in
modifications of marine or land beings can be appreciated only at very
long distances of time. Gradual changes of this kind seem to have pro-
gressed during the whole period of the Cretaceous formations of the West,
from the base of the Dakota group to that of the Tertiary Lignitic, and
later still ; for in the whole vertical space occupied by the deposits no
unconformability of strata is remarked. But the concurrence of gradual
atmospheric modifications with those of the earth surface is distinctly
recognizable in the general character of the flora of the lower Lignitic
compared to that of the Dakota group, this being of a temperate
climate, while that of the Lignitic proves a subtropical one. Of course
the life under deep seas cannot be modified in the same degree and in the
same period of time. It is but very slowly influenced by land atmospheric
changes, and from this there is in some instances between the in-
habitants of the land and those of the sea, a forcible geological discord-
ance, like that exposed at Black Butte by the Saurian and the plant's
remains wherein it was imbedded.
Perhaps the more weighty objection against the deductions taken
from the characters of the Lower Lignitic flora is that of the unreliability
of comparison between the vegetable tyi)es of both continents in their
relation to supposed synchronous epochs. From this objection it is
said that we should not attempt, in regard to the distribution of the
North American fossil plant, to consider anything known of the geo-
logical relation of those of Europe. This objection appears at first
trifling, and it seems that it could be answered by the mere assertion that
as American paleontologists have constantly taken their points of com-
parison from Europe, in considering the relation of the animal remains
to the age of the strata, where they were discovered, vegetable paleon-
tology should be allowed to use the same privilege ; for no section of
natural science can be defined and progress a priori or without means
of comparison, and where to And any if the European scientific do-
main should be closed. But in this objection there is something more
than the mere privilege of comparison. It seems positive that from its
i^guKBEux.] EVIDENCE OP AGE OP LIGNITIC GROUP. 295
first appearance the Americau land iSora has a proper American cbnracter,
recognizable not merely in diftcrence8, but in priority of types. • I have
already allnded to this phenomenon, which, though seemingly observ-
able in many instances, is, however, not positively ascertained as an
actuality, and not referable to a principle of a general application. We
have, as far as our knowledge goes, a precedence of vegetable Devonian
types which are already oeen in the Silurian ; the Carboniferous, also,
are recognized by remains of Lepidodendron as low as the Marcellus
epoch. The Sub-Carboniferous flora of this continent is mostly Devonian
for Europe, and the Lower Carboniferous has a number of specific forms,
considered by European authors as Permian. Farther up, the Trias is
Jurassic by its Cycadece^ and the Cretaceous of the Dakota group is
typically allied to the Miocene species, and still more to the present
flora of this country. If it is so, the objection expressed above is a
mighty one, for then our Lignitic flora might be of an older period and
representative of an American Cretaceous formation, though having
already the characters of European Eocene floras t We have, in this
peculiar case, a point of reliable comparison which answers the ob-
jection. The flora of Point of Bocks, considered as Tertiary, is prob-
ably at the lowest stage of the formation. Its characters have been
exposed in a table of comparison. Now, the floras of Gelinden, in
Belgium, and of S<6zanne, in France, are connected with strata ac-
knowledged by stratigraphy and animal paleontology as of the oldest
European Tertiary. And here as at Gelinden, for example, the Creta-
ceous type, represented by Bryophyllum^ is far more evident than at
Point of Bocks, and in the flora of Suzanne it is about in the same
proportion as in that of Point of Bocks and Black Butte. In this
<^se, therefore, no trace of precedence of vegetable types is remarked on
this side of the Atlantic, and the floras of both continents, ofifering
evident synchronism by stratification, and both animal and vegetable
paleontology, may be considered as giving reliable evidence by the
comparison of tbeir characters.
It is claimed that the opinion on the Tertiary age of the Lignitic
contradicts evidence admitted by the highest scientific authority.
Though no personal opinion may be recognized as authoritative in
science, we have, on the question discussed here, a concurrence of
views expressed by Dr. Newberry for the Lignitic flora of the Union
group of the Upper Missouri Biver, and by Prof. J. W. Dawson
for that of Canada. These are certainly the highest authorities in
this country. From Europe, the opinion of Count Saporta, who is
deeply interested in tbe progress of the botanical paleontology of this
country, is not less explicit. After the examination of some of the
plates prepared for tbe flora of the Lignitic, he writes: '<That
Sphenopteris Eocenica is closely allied to A^plenium Wegmanni, Brgt.,
of Suzanne; that species analogous to what I have described as
Abietitea dvhiua and Abietites setigera have been found in the Upper
Cretaceous of St. Paulet, France ; that our Palms, especially PalmaciteH
Goldianus, denote Eocene ; that the magnificent species Sabal Grayana
is allied to, and perhaps an ancestor of, Sabal majors which in Europe
ap])ears at the beginning of the Miocene; and that ^/abeUaria communis
is extremely similar to Sabal andegavienaiSy which is found in tbe Eocene
Superior of the south of France, but which has not been figured till
now." From all this and other points of afi^nity which the cele-
brated paleontologist of France makes in regard to the species of the
lower group of the Lignitic flora, he concludes as follows :• — " In re-
• In letter, October,19, 1875.
296 GEOLOGICAL SURVEY OF THE TEBBITORIES.
suraiDg, and Dotwithstanding that Abietiies^ which I consider as a Cre-
taceouA type, your first group seems indeed to be legitimately Eoeecc,
by its Ferns, its Palms, its coriaceous and prototypical Poplars, its
Cinnatnomumj and its Vibumunij as related to the Suzanne flora, and by
one of its Palms to the Upper Eocene of Angers. If one would suppose
this flora more recent than the Eocene, he would have to admit soch a
dissemblance between Europe and America that every comparisoo by
the floras between the geological stages of both continents should ap-
pear an impossibility." The assimilation of American species with a
number of Miocene species published in Europe is considerod by Saporta
as doubtful and not quite conclusive ; and he remarks, also, that, though
his opinion on the age of the Lower Lignitic group is given aocording
to present impression, the great geographical distance renders the
affinities between compared localities very difficult to fix with precision,
even in supposing them contemporaneous.
These quotations must be excused by reason of the importance given
now to the question of the age of the Lignitic, which, controverted in
various ways, demands light, and has to be considered in every possible
point of view. The problem is not yet solved. Eequested, as I am, to
contribute a share in the discussion, by closely adhering to paleontologi-
cal evidence, and exposing it as far as it is given by fossil plants, I had
to enter into details in order to show its weight. And no better oppor-
tunity could be afforded for this purpose than a review of the group of
plants obtained from Point of Eocks by Dr. Hayden.
From the following descriptions it will be remarked that some of the
specimens have been found and communicated to the survey by Mr.
William Cleburn, of Omaha, a zealous explorer and student of the vege-
table paleontology of the Western Territories.
Description of species of fossil plants from Point of Eocks.
\\ 1. FUCUS LIGNITUM, «p. nov.
Frond flattened, irregularly dichotomous; branches diverging ob-
liquely ; branchlets short, terminal, linear-divaricate, tufted, forking at
the point.
The fragment figured is the only one of this kind in the specimens. It
represents a species allied to SpJicerococcus crispiformis^ Sterub., as de-
scribed in fleer's Flor. Tert. Helv. (p. 23, Pi. IV, fig. 1), and still more,
perhaps, to the living Fueuscanalieulatus^ Agh., very common along the
coasts of the Baltic Sea, and also discoverd in numerous specimens in
the Tertiary of Spitzbergen. The base of the lowest branches is four
millimeters broad, but the size of the branchlets diminishes nearly one-
half at each dichotomous division. The terminal branchlets are only
half a millimeter broad, fasciculate-dichotomous, short, split, or furcate
at the point, and divaricate. The substance appears thin, membrana-
ceous, and yellowish.
flABiTAT. — Point of Eocks, Br. F. F. Hayden.
K 2. Salvinia attbnxjata, sp. nov.
Leaves small, one centimeter or less in diameter, opposite, joined at
the narrowed, slightly-pediceled base, round or broadly oval, indis-
tinctly reticulate by vertical and parallel rows of quadrate, large cells,
marked in the middle by black spots, formed by very small, close cells,
or pores, without any trace of a middle nerve.
This fine species is related by its reticulation and its size to Salvinia
Mildeanay fleer (Bait. Flor., p. 17, PI. Ill, figs. 1 and 2), differing from
LE8QUBEEUX.1 FOSSIL PLANTS FROM POINT OF ROCKS. 297
it by broader, less distinct, square areolsB, the absence of a dividing
middle nerve, and the narrowing of the base to a very short pedicel.
By these two last characters, this species is nnlike any of this genus.
It is, however, probable that the two leaves representing it were not,
when embedded into the clay, in their full state of maturity, one of
them being smaller than the other, and its areolation far less distinct.
In the young leaves of the living Salvinia natans^ the leaves, l>efore
attaining their lull development, have the middle nerve scarcely dis-
cernible.
Habitat. — Point of Bocks, William Cleburn.
K3. S£LAGIN£LLA t FALCATA, 9p. nov.
Frond small, dichotomous ; pinnse narrow-linear, one to four centime-
ters long, six to seven millimeters broad ; pinnules close, two-ranked,
in right angle to the rachis, generally covering each other at the bor-
ders, falcate upwards, lanceolate-acuminate, suddenly narrowed to the
point of attachment, without distinct middle nerve.
I have figured four different parts of this plant, which is abundantly
scattered among the floating rootlets and upon the specimens of the
Lemna f Scutata. It may represent some kind of floating fern, per-
haps, rather than a species of Selaginella. It is, however, closely
allied to Selaginella BertJioudi, Lsqx., described in Dr. Hayden's Annual
Beport for 1873 (p. 395), differing, however, by the two-ranked position
of the leaves and their distinctly falcate form.
Hajbitat.— Point of Bocks, Dr. F. V. Hayden, TF. Cleburn.
One of Mr. Cleburu'a specimens represents a fragment of a stem ten
centimeters long, one centimeter broad, round, but flattened by com-
pression, covered with densely imbricate leaves of the same form and
size as those of the branches. This stem proves the relation of the
described fragments to the lyoopodiaceous family.
K4. Selaginella laciniata, sp. nov. t
Branches dichotomously divided ; divisions two to three centimeters
long ; leaflets f opposite, distichous, divided from the base in three to
five filiform laciuise, some of them forking at the middle, all curving
upward, or falcate.
By its mode of vegetation, the form and divisions of the pinnsB or
branchlets, these small plants are exactly similar to those described
from Dr. Hayden's specimens under the name of Selaginella falcata.
The difference is in the remarkable laceration or thread-like divisions
of the leaflets. The laciniaB distinct and in relievo upon the stone are
like the veiulets of fern -leaves, when, by maceration and decomposi-
tion, their epidermis has been destroyed, or like skeletons of leaves. In
this case, however, as these thread-like branches are more or less nu-
merous, either simple or forking from the middle, and thus differing in
number and mode of divisions for each leaflet, this appearance cannot
result from decomposition in water. It is probable that these remains
represent a kind of lyoopodiaceous plant, living sometimes partly im-
mersed, and that, as it happens in numerous species of water-plants of
this epoch, the immersed leaves become decomposed, and grow into la-
ciniate divisions, while the emerged ones are entire or undivided. This
difference in the leaves is particularly marked in Kaaturtium lacustre^
Gray, known to every botanist. I do not know, however, any Lyco-
podium species shovf ing this kind of variations in leaves. Even L. in-
undatum has the leaves of the immersed part entire or without divis-
298 GEOLOGICAL SXTEVEY OF THE TEBRITOEIES.
ions. It is therefore uncertain if the specific separation of these fiag-
ineiits is authorizable.
Habitat. — Point of Rocks, William Clebum,
^ 5. Sequoia bbeyifolia, Heer.
Branches fiexaous; branchlets opposite or svlternate, open and diverg-
ing near the base, then carving upward and erect from the middle to
the top. Leaves of two kinds, either small, short, scaliform at the base
of the branchlets and covering the whole of them when young, or oblong,
enlarged in the middle, obtuse or abruptly narrowed to a point, and
gradually and slightly so toward the decurring base, distichous, oblique,
decreasing in length toward the base and the top of the branchlets.
We have a large branch* and numerous more fragmentary sfiecimensof
this fine species described by Ueer in Flor. Arct (p. 93, PL II, iig. 23),
from Greenland specimens, in Flor. Spitz, (p. 37, PI. IV, figs, 2-3), from
Spitzbergen specimens, and formerly in Fl. Baltica (p. 21, PI. Ill, fig. 10).
It is well characterized by the form of its generally short open dis-
tichous leaves, either abruptly pointed, or obtuse, deeply nerved, and
slightly decreasing in width from above the middle to the base. We
have, however, a number of specimens with somewhat narrower, nearly
linear, longer leaves, which show a notable deviation of the normal form.
The cone of this species is not known as yet. One of the specimens bear-
ing scattered branchlets and leaves of this Sequoia has a cone, which
api>ears to be a flattened cross-section, or perhaps the flattened base of
the cone turned upward, the pedicel marking the central point around
which the scales, oblong, cuneate, narrow, emarginate at the top, are im-
bricated to the borders. These scales rather resemble those of a Offp-
tostrohus than those of a Sequoia.
Habitat.— Point of Rocks, Dr. F. V. Hayden^ Wm. Olebumy whose
collection has about one-half of the specimens representing this
species in its normal form, and its variety.
^\6. Sequoia longifolia, Lsqx., MSS.
Branches thick ; leaves closely appressed, erect, long linear lanceolate-
pointed or accuminate, enlarged above the slightly contracted and decur-
ring base ] scars deep, lingulate-pointed, marked by a deep groove in the
middle.
This species was already described from Black Butte specimens ; these
have, some of them at least, longer leaves than those of Black Butte. In
these, the leaves average two and a half to three centimeters long aud
three millimeters wide ; in those of Point of Rocks, the leaves, of the some
width, are generally five centimeters long, even more. In both forms,
they are marked by a broad indistinct middle nerve, and the surface,
seen with the glass, appears very thinly striated in the length. This char-
acter, as well as the thick consistence of the leaves, seems to prove the
identity of the species, though the leaves of the specimens of Point of
Rocks are not only longer but proportionally narrower and scarcely
contracted to the point of attachment to the branches. In both, these
leaves are generally crowded and covering the stem.
Habitat. — Point of Rocks, Dr. F. V. Hayden.
I \ 7. Sequoia tiformis, «p. nov.
Stems thick, pinnately branching ; branchlets short, obliquely di-
verging ; leaves either linear or somewhat broader in the middle, grad-
* A beautiful specimeu, the property of Mr. £. H. Clarke, agent of the Union Pacific
Railroad, who kindlj lent it for illustration of the species.
ULSQUBRiux.] FOSSIL PLANTS FROM POINT OF ROOKS. 299
unlly narrowed to a point, slightly contracted to the decnrrent base,
slightly incurved or falcate, sometimes erect and appressed to the stem;
scar-leaves triangular or liugnlate pointed.
This species apparently bears two kinds of leaves, even upon the same
specimens; either long, two centimeters, and very narrow-linear, less than
one millimeter wide, or shorter and broader, decreasing gradually from
the base to the point, linear-lanceolate, nearly oneand one-half millime-
ters wide and only eight to ten millimeters long; the middle nerve is
deeply marked upon both kinds of leaves. I should have considered
the numerous specimens bearing branches of this Sequoia as represent-
ing two species, the one with narrow longer leaves, the other with shorter
broader leaves. But even the diflference in the length and proportion-
ate width of the leaves is distinctly perceivable upon one of the speci-
mens, and the difference also in the length of the leaves, all narrow and
of the same width, is evident upon another. There are, moreover, a
large number of specimens, all fragmentary indeed ; and the difference
in regard to the size of the leaves is apparent upon most of them. In
the average, the leaves are much narrower than those of Sequoia Beich-
enhachi^ Heer, to which this species is related by the falcate form of
some ot the leaves.
Habitat.— Point of Bocks, Dr. F. F. Hayden.
>f8. WlDDRINaTONIA COMPLANATA, 9p. nov.
Stem thick, disticho-pinnate ; branchlets short, thick, alternate, ob-
liqne; leaves small, in spiral order, closely imbricate and appressed,
oblong-lingulate pointed upon the primary branches, ovate-pointed or
rhomboidal and shorter upon the obtuse branchlets.
This species, represented by many specimens, is evidently related to
Widdnngtonia antiqua (Sap. Et., 2, 1, p. 69, PI. I, fig. 4), for the form of
the leaves, which are, however, more closely appres^dd in the American
species, and more distinctly placed in spiral order around the branch-
lets. These leaves do not appear of a thick substance, the coat of
coaly matter over them being extremely thin.
Habitat.— Point of Bocks, Br. F. F. Hayden^ William Cleburn.
K9. PiSTIA COEBUGATA, 8p. noV.
Leaves thick, at least toward the base, varyingin diameter from two to
three and one-half centimeters, broadly obovate, generally bordered from
above the base by a wavy margin two to five millimeters broad ; gradu-
ally narrowed into a short pedicel about three millimeters thick, termi-
nating into a bundle of radicles; veins emerging from the pedicel in two
or three thick bundles, dividing and diverging from the base of the
leaves, atid forming in ascending, by a kind of abnormal anastomosis,
irregularly polygonal meshes.
These leaves, resembling in form a small bladder, contracted on one
side, seem somewhat inflnted, or at least thickened, from the base to
above the middle, or composed of two distinct areas, the lower one cir-
cular and separated by a narrow groove, or deep line, from the wrinkled
border which surrounds it, narrowing, however, gradually toward the
pedicel. The areolation of this border seems disconnected and distinct,
representing large quadrangular areolae, whose subdivisions cnrve along
in festoons. Sometimes, however, the central part is not inflated, or
thicker, and in this case, as in specimens representing .voung leaves, no
traces of borders are perceivable. This groove, therefore, and the sep-
aration of the leaf in two distinct parts, may be caused by a kind of fold
300 GEOLOGICAL SURVEY OF THE TEBRITORIES.
around a tergescence of the lower part, formed by au abnormal growth
of radicles. The upper surface of the leaves is somewhat rough ; the
lower surface, inside of the fringe, is dotted with minute holes, or like
spongious. The leaves are generally mixed, or superposed to thin foli-
form long radicles, all of the same size, coming in bundles from linear
rootlets, two to five millimeters thick. They form a thick coating sor-
rounding the leaves, or whereupon the leaves Are floating, without evi-
dent connection or point of attachment to them.
At first I supposed these leaves as representing the same species as
the following, but their relation to species of Pistiaj whose leaves are flat
and not like vesicles, seems to indicate, though the likeness in some of
the characters may be, that these organs represent two kinds of water-
plants. Comparing this one to leaves of Pistia spathtUata^ Mich., from
specimens of Louisiana, the affinity is remarked not only in the obovate
sha[>e of the leaves, but in the kind of nervation, by inflated primary
veins diverging from the base of the pedicel, where they pass into bun-
dles of radicular filaments of the same characters as those of the fossil
plant. Most of the leaves of the living species, the old ones especially,
bear from the middle to the base an inflated spongious coating similar
to that which is observed on the under surface of the fossil leaves. The
more marked difiereuce is in the central part of the fossil species, which
appears surrounded by a distinctly-marked deep line, while in the leaves
of P. spathulata the thick zone, though definite, terminates in passing up-
ward along the primary veins ; but this diflerence, like that of the areo-
lation along the borders, is specific only and the generic identity appears
clearly defined.
Habitat.— Point of Rocks, very abundapt, and covering by itself only
large surface of shale. Dr. F» V, Hayden^ Wm. Clebum.
«
MO. Lemna Scutata, Daws.
Fronds round, entire, slightly undulate on the edges, sometimes an inch
in diameter, single or grouped ; roots numerous, filiform, proceeding
from a round spot near the notch of the frond.
To this species, as described and figured by Professor Dawson (Report
on the Geology of the Forty-ninth Parallel, Appendix A, p. 329, Tab. XVI,
figs. 5 and 6), I refer a number of round bodies, leaves or fronds, mixed
. with the species described above. Comparing them with the author's
figures, there is no difiereuce whatever, except that if some of them do
not show any trace of veins, others, exactly of the same shape, are
veined from the base, where the radicular filaments are attached to them
and the veins distributed as in the former species. Some specimens also,
one of which has been figured, show the basilar part inflated, or the
l>edicel wherefrom the veins are diverging, just in the center of the cir-
cular organism, as if it had been a bladdery or vesicular plant, flattened
by compression. I still believe that both the leaves described above
and these represent the same kind of vegetable, these being the young
and yet undeveloped organs. All the different appearances of these
plants, represented by numerous specimens, have been figured, and the
comparison of their various forms will, I think, satisfy paleontologists
in regard to their relation to a species of Pistia.
Habitat.— Point of Rocks, mixed with the former, I>r. F. V.Eayien^
Wm, Cleburn.
-Ml. Ottelia Americana, «p. nov,
Spathe ovate narrowed to a round pedicel, surrounded by an undu-
lated and wrinkled fringe, emarginate at the top.
I-E6QUBRBUX.1 FOSSIL PLANTS FBOM POINT OF BOCKS. 301
The central part of this organism, representing the spathe of a water-
plant, is oval, somewhat inflated, narrowed to a round pedicel, and sur-
ronnded by a margin or fringe half a centimeter broad, cut or emargin-
nte at the top. The middle part is slightly inflated and striate in the
length. The border fringe is opaqne, and does not show any ap-
l>earance of nervation. Comparing it to a figure of OtteliaalisfnoideSj
I*ers., from Ceylon, kindly communicated by Saporta, the fossil plant
Beems in perfect concordance of characters with the living.
Habitat. — Point of Eocks, Dr. F. V. Hayd^ represented by one
specimen only, in a good state of preservation.
Vvj.2. Sabal Gbayana, Lesqx. ^ /
Trans. Am. Philsoc., vol. xiii., p. 412, T. xiv., figs.4-6.
Frond apparently large, represented by fragments only ; rachis flat,
elongated linear-acuminate, six to eight inches long, enlarged at its
base and rounded on both sides ] rays numerous, gradually enlarging
upward, half to two and one-half centimeters broad, marked with dis-
tant and distinct slender veins. The characters of this species have
been described in detail as quoted above. The species is always easily
identified by its slender though distinct and equally distant veins.
Habitat. — Point of Rocks, Dr. F. V. Hayden.
Kl3, Deyophyllum ceenatum, ap. nav.
Leaves oblong, lanceolate, abruptly oblique to the petiole or subtrun-
cate ; borders deeply, regularly crenate ; substance of the leaves some-
what thick, subcoriaceous ; surface rough ; nervation pinnate, middle
serve flat and broad, lateral veins diverging sixty to sixty-five degrees,
•flat, distinct, slightly curving in ascending to the borders subcampto-
drome, the veins forking up under the sinuses of the teeth, and a branch
passing up along the borders from the point where the veins enter the
teeth ; nervilles thick, in rightangle to the vein's, forming, by subdivision
and anastomosis, a square or indistinctly polygonal areolation.
Of all the species described of this genus, none is comparable to this
one, which is especially distinct by its broadly obtusely dentate borders.
It is represented by two fragmentary specimens.
Habitat.— Point of Bocks, Dr. F. V. Hayden.
Vl4. Dbyophyllum subfaloatum 8p. nav.
Leaf subcoriaceous, linear-lanceolate, acuminate or sharply pointed :
borders regularly serrate with short blunt teeth turned upward ; lateral
veins parallel, diverging thirty to forty degrees, straight to the point of
the teeth ; fibrillaB close, thin but distinct, simple or ramified in the
middle, the upper ones joining nearly in right angle, a branch veinlet
which pass from near the point of the lateral veins tundev the sinuses, and
follows along and close to the borders.
There is only a fragmentary specimen of this species, the upper half
of a leaf. By its form and nervation, it seems at first referable to the
' genus Castaneay and, truly, it would be easy to find leaves of the present
C. v€8ca apparently perfectly similar to this fossil one. There is, how-
ever, a difference in the areolation, or in the arrangement of the tertiary
veins. In these primary types of Quercus and OiMtanea described under
the name of Dryophyllum^ the upper branch of the secondary veins
passed from near the i)oint of the vein under the sinuses and closely
follows the borders, which thus sometimes appear narrowly marginate,
and is joined nearly at right angle by the upper fibrillre. This charac-
3U2 GEOLOGICAL SURVEY OF THE TERRITORIES.
ter, though still iudistiDctly traced io the leaves of Castanea^ aod of
some species of chestua^oaks, is far less regular, the apper braacb«s
which follow the borders beiug of various sizes, not so exactly intralld
to the borders, and not in close proximity to them. This new siteeiesis
intimately related to DryaphyUum DewdUquei Sap. & Mer. (Flof* de Qe-
linden)^ especially to the fragment figured in PI. Ill, Fig. 2. It differs
only by the shorter, less acute teeth of the borders, the slightly falcate
form of the leaf, and the close thin fibrillar.
Habitat. — Point of Bocks, TTm. CMmm.
f\15. POPULUS MBLANARTA, Hccr.
Leaves with a long, slender petiole ; deltoid, subtruncate at base ;
borders acutely serrate ; primary basilar lateral nerves emerging from
above the border base of the leaf, with a pair of thin marginal veinlets
underneath.
Considering what can be seen of this leaf from the fragment which
represents merely its lower half, with the long, slender petiole, the dis-
tinct nervation, and a few of the border-teeth, it exhibits characters in
accordance with those described above, and translated from Schimper's
Vegetable Paleontology, and especially with the figure given of this
species in Flor. Tert. Helv. (PL LIV, fig. 7). Professor Herr remarks,
that it essentially differs from Populm latior^ var. subtruncata^ by the
position of the lateral primary nerves at a distance from the border-base
of the leaves. In the leaf figured as indicated above, this distance is
still greater than in that in the Flor. Helv. Heer remarks also that
he has seen a large number of specimens of the same species, but that
in all except one, which he has figured, the upper part of the leaves
was destroyed, as it is in ours. He mentions as distinctive characters,
the acutely serrate borders of the leaves, and the middle nerve thicker
than the lateral ones, the same as seen upon our specimen. I have,
therefore, no doubt about the relation of this leaf to the European
species.
Habitat.— Point of Bocks, Dr. F. V. Sayden.
\^).6. POPULUS MELANARIOIDES, «p. flOV.
Leaf subcoriaceous, nearly round, subtruncate at base, long-petioled ;
borders undulate ; nervation ternate from above the base of the leaf,
secondary veins two pairs, at a great distanee from the primary ones,
these much branched outside ^ the others simple, all the divisions pass-
ing to near the borders, where they become efiaoed in the areolation;
nervilles thick, flexnous, in right angle to the veins, forming by raoii^
fication at right angle square polygonal meshes.
By the su^oriaceous substance, the long slender petiole of the leaves,
this species is referable to the section of the Trq^ida (Trembling P<^
lars). As in Populus tremulafolia, Sap. (Et, 3^ 2, p. 26, PI. lU, fig. 4),
to which this species is allied, the veins and their branehes pass through
the areas to very near the borders, which they seem to reach. Tlie
American form differs merely by less-distinctly undulate borders, the
distance of the primary lateral nerves above the base, and by the great
distance of the secondary veios. These two last characters are, how-
ever, of no moment for the speoifieation of poplar-leaves, as can be n-
marked in the examination of a few leaves of the too oomHMm Popuha
aUba. In fossil species, Po/pulm JfoMiiieiwis, Sap. (Bt, 3, 2, p. 30, PI. Iff
fig. 6), is represented by three leaves, each of a different character of
nervation. The relation of this species with that of the Tertiary
LE8QUBRBUX.] FOSSIL PLANTS FROM POINT OF ROCKS. 303
(Miocene?) of Provence, described by Saporta, may be therefore more
intimate than it appears from the comparison of a single leaf. Our
species is also comparable to Populm heliadumy Ung., by its form, and
to P. melanariaj Heer, by its nervation.
Habitat.— Point of Rocks, Wm. Clebum.
^17. FlOUS ASAKIFOLIA, Ett
Leaves petioled, broadly reuiform, sabcordate or subpeltate, very
obtuse, small, with borders crenalate ; primary nerves palmately five
to seven ; middle nerve straight ; upper lateral ones strong, curving
inward, branching and anastomosing with the upper secondary veins;
Teinlets transversal, their ramification forming a protuberant, or em-
bossed, very distinct, polygonal areolatiou.
Though this species has been already briefly described from speci-
mens found at Golden, in Dr. F. V. Hayden's report for 1872 (p. 378), it
had as yet not been figured, the fragments of leaves being generally
too incomplete. It is, however, easily recognized by its peculiar nerva-
tion, forming small, elevated, polygonal areolse, an areolatiou like an
embossed checkerboard, resembling that of Asarnm JSuropeum, The
fragments of Golden seem to be part of much larger leaves than those
of Ettinghausen, who described the species in Bilin Flora (p. 80, PI.
XXV, figs. 2-3). These per contra^ from specimens of Point of Eocks,
are perfectly well and entirely preserved leaves, rather smaller, except
one, than the leaves of Bilin. They are also slightly more expanded
on the sides, or reniform, and the crenulations less distinct, but these
border-divisions are, for their size, related to the areolation, which is
wider in proportion of the size of the leaves. Our leaves, also, are
evidently peltate, at least in two of the figured specimens. One only
has the position of the thick petiole marked similarly to that of the
European leaves ; but even the representation of the species by the au-
thor seems to indicate peltate leaves, whose borders are erased at the
base or at the point of attachment of the petiole. The differences are
too unimportant to be consideii»d as specific characters. These leaves
merely represent a local variety, or a var, minor. This species appears
to be rare in the Tertiary of Europe, as it has till now been seen only
in the plastic clay-beds of Bilin.
Habitat.— Point of Bocks, Dr. F. V. Eaydsn^ Wm. Olebum.
^18. Ficus Dalmatica, Ett
Leaves narrowly ovate, obtusely pointed, narrowed to a short petiole ;
middle nerve thick toward the base, thinning upward ; basilar lateral
nerves, from above the border-base of the leaves, thin, ascending at an
acute angle of divergence of thirty degrees to the middle of the leaf;
secondary veins more open, equidistant; nervation camptodi'ome, joined
by transverse nervilles.
In considering the figure by the author in Flora Promina (PI. YII, fig.
11), there is no difierence whatever between the European form and
ours; but the description says that the secondary veins are branching
at the point, and there is no trace of divisions of veins observable upon
oar specimens. As, however, the figured single leaf shows merely trans-
verse nervilles and not real branches, and as these nervilles are also
visible on the American form, it is apparently identical. One of the
leaves represented in our plate seems rounded at the base. This is
caused by its reversement into the stone, the upper part cf the leaf be-
ing flat and tbe lower carved down in entering the stone where the
extreme base and petiole are imbedded.
Habitat.— Point of Bocks, Dr. F. V. Eayden.
304 GEOLOGICAL SURVEY OP THE TERRITOEIES.
^J9. Ficus Planicostata, Lsqr.
Dr. F. Y. Hayden's Report on the Geol. Survey of the Terr. 1872, p.
393.
A small leaf in a perfect state of preservation represents this spe-
cies very common at Black Butte. It is easily recognized by the broadly
ovate, thickish, entire leaf, slightly pointed or obtuse, rounded or sub-
cordate at base, short-petioled, three-nerved from the top of the petiole,
&c.
Habitat. — Point of Eocks, Wm. Clehum.
f\20. Ficus Tili^folia, Heer.
Like the former, it has been described previously in Dr. F. V. Hay-
den's Eeport for 1871, p. 287, from specimens of Washakie station ;
mentioned in supplement to this report, p. 12, from Evanston ; p. G,
from Placi^re anthracite ; in same report, for 1872, p. 375, from above
the Gehrnngs coal, near Colorado Gity ^ and p. 393, from Black Butte
station. We have also specimens from Golden and other localities ; for
here, as in the Miocene of Europe, this fine species, so easily identified,
is distributed through the whole thickness of the Lignitic, excepting,
however, the upper stage, that of the Green Eiver group, where it has
not been found as yet. I have figured it from specimens of Point of
Eocks, not merely because it is there clearly represented, but to show
more evidently the relation of this locality with the Tertiary Lignitic.
Habitat.— Point of Eocks, Dr. F. V. Hayden.
rV21. Ficus irregularis, Lsqx.
This species was published under the name ot Ulmusf irregularis^ in
Dr. F. V. Hayden's Eeport for 1872 (p. 378), the generic reference being
then uncertain. Numerous specimens obtained later from Black Butte,
where the species is common, shows a thick inflated leaf-stalk, a char-
acter which indicates the relation to Ficus. The specimen of Point of
Eocks is like the counterpart of one already engraved fix)m Black Butte
specimens; the identity of characters is unmistakable, and therefore it
was flgured also as another recoi^d of identity of the flora of both local-
ities.
Habitat.— Point of Eocks, Dr. F. F. Hayden.
\\22. TrapaT microphylla, «p. nov.
Leaves small, round, or broadly oval, obtuse, rounded to a short peti-
ole, with borders denticulate from below the middle, three-nerved from
the top of the petiole, or irregularly pinnately nerved ; lateral veins at
an acute angle of divergence, fifteen to twenty degrees, fleznous, with
dichotomous branches, all craspedudrome ; areolation by subdivision at
right angle, polygonal, distinct.
These leaves vary in size from a little more than one centimeter long
and nearly as broad to about two and a half centimeters long and nearly
two centimeters broad. They are generally oval-obtuse, somewhat en-
larged toward the round point ; the borders are minutely dentate except
at and near the base, rounded to a comparatively long and slender peti-
ole, the only one of the leaves where it is preserved being eighteen milli-
meters long, and its petiole nine millimeters. The areolation is peculiar,
in square or polygonal areolse, formed by close, thick nervilles, aoasto-
mosing with veinlets parallel to the veins and their divisions, the areola-
tion being clearly defined, and the parietes as thick as the veins. The
same kind of areolation is remarked upon the lower surface of the leaves
uMQUBEBux.] FOSSIL PLANTS PBOM POINT OP ROCKS. 305
of Trajpa natans^ which, though comparable to the fossil ones by the areo-
la t ion, has its borders deeply toothed and a mach thicker consistence.
Id this species, the leaves appear membranaceous and as pellucid, so
distinctly marked in black appear the nervation and the areolation
upon the yellowish substance of the leaves. These leaves are mixed with
the filaments oT rootlets described with Lemnaf bullataj and represent
evidently a kind of water-plant. No fossil leaves published as yet are,
to my knowledge, comparable to these, except those described by Pro-
fessor Newberry, in the Report of the Colorado Exploring Expedition
by Lieut. S.O. Ives (p. 131, PI. Ill, fig. 5), under the name of Neuropteris
angulata. The outline or general form of the slightly dentate leaves, the
pinnate nervation, and the remarkably acute angle of the secondary
veins are characters common to both species; even the irregular though
oo o bscurely marked division of the secondary veins seems to be of the
same kind, it may b& remarked that Professor Dawson has observed
and described a fruit of Trapa found in connection with his Lemna scu-
tata; therefore in circumstances similar to those where these leaves,
referred to Trapa^ are found.
Habitat. — Point of Bocks, Dr. F. F. Hayden, Wm. Clebum.
tf23. Laurus (Pbbsea) pb^stens f , sp. nav.
Leaf coriaceous, large, broadly lanceolate or elliptical, narrowed up-
ward to an acute point, and downward in the same degree to a thick,
short petiole; middle nerve thick; secondary veins strong, parallel;
uervilles distinct ; areolation very small, lightly marked.
The very fine and well-preserved leaf is sixteen centimeters long from
the base of the thick petiole, which is one centimeter long, five centi-
meters broad in the middle, where it is the widest, and has thick sec-
ondary veins regularly branching, with distinct uervilles and the areo-
lation of a Laurus, The foliaceous substance of the lower part of the
leaf is debtroyed, bat the middle thick nerve and the petiole are pre-
served, as well as the outline-borders. By its nervation, this species is
allied to Persea speeiosay Heer, diifering by the form of the leaf and the
thick middle nerve. By these two last characters, it is comparable to
Xaitrti* |>ri»cep«, Heer (PI. Tert. Helv., II, p. 77, PI. XC, tigs. 17-20),
differing, however, by the secondary veins somewhat thicker and slight-
ly more distant. It is most closely related to the present Laurm Can-
ariengiSj Sm.
Habitat.— Point of Bocks, Dr. F. V. Hayden.
K24. Viburnum EOTUNDiFOLiUM, «p. luw.
Leaf nearly round, small, surrounded by a block bordor, slightly'' and
distantly denticulate by extension of the borders at the point of contact
of the secondary veins and of their branches, all craspedodrome ; sec-
ondary veins open, diverging fifty to sixty degrees, equidistant, parallel,
the two lower pairs ramitied, the upper ones only forking near the bor-
ders; areolation distinct, from parallel distant fibrilise, branching and
anastomosing in large equilateral meshes.
The black borders of the leaves, the general characters of nervation,
and the facies are the same as in the other species of Viburnum pub-
lished from Black Butte. This leaf differs especially by its nearly round
form, the base rounded to the petiole, the secondary veins more open,
and especially the very small, slightly-marked teeth of the borders. But
for this last character, this leaf could be referredto Vihumumplatanoid^s,
Lsqx., as represented by the small leaf of PL XXXVIII, fig, lOy of the
20 H
306 GEOLOGICAL SURVEY OF THE TERRITORIES.
inecl. Lignitic Flora. Iq this, the secondary viens are, however, more
oblique aud more distant. It may be a mere lociU variety.
Habitat. — Point of Bocks. Dr. F, V. Hayden.
V\25. ViBUBNTTM Wympbri, Hecr.
This species has been described in Dr. F. V. Hayden's Report for 1873,
p. 382, and referred, with some doubt, to the Greenland species described
in Arct. Fior. (II, p. 475, PL XLVI, tig. 1**). The secondary veins in oar
species are more distont and less regularly parallel. Though its rela-
tion to the arctic species is somewhat doubtful, it does not show any
difference whatever from that of Bhick Butte.
Habitat. — Point of Rocks, Dr. F. V, Hayden.
'^\26. ViRBUBNUM marginatum, Lsqx.
The specimen is fragmentary, but the species, very common at Black
Butte, is recognizable.
Habitat.— Point of Bocks, Win. Clebum.
N\27. DiosPYROS BRA0HYSEPAL4, Al. Brauu.
Described already in Dr. Hay den's lieport for 1872 (p. 394), from spe-
cimens of Black Butte, and in Report for 1873 (p. 401), from specimens
of Sand Creek, Colorado, a locality identified with Golden by its flora.
But none of the leaves found as yet are as well preserved and as well
characterized as that of Point of Bocks, which is especially comparable
to the leaves in Heer's Fl. Tert. Helv. (PI. CXI, fig. 2). The species is
not rare in the Miocene of Europe, especially in the lower groups^ and
appears equally widely distributed in our Lower Tertiary.
Habitat.— Point of Rocks, Dr. F. V. Hayden.
K 28. Greviopsis Clebxjrni, «p. nov.
Leaves of medium size, subconaceous, ovate, rounded, and narrowed
by an inward curve to the short petiole, sinuato-denticnlate, three-nerved
from above the base; primary veins thick; secondary veins, two or
three pairs, distant from each other, and also from the primary nerves,
all branching outside with subdivisions or veinlets entering the teeth ;
nervilles in right angle to the veins, llexuous, simple, or branching in
the middle ; areolation obsolete.
This flue leaf, about five centimeters long (the point is broken), fear
centimeters broad in its widest part, below the middle, is so remarkably
similar by its form, the denticulate borders, and the nervation, to Oreti-
opsis orbiculata^ Sap. (Sezane Fl., p. 411, PI. XI, figs. 11 and 12), tbat its
generic identity is positive. It specifically differs by its larger size, tbe
more distant veins, and the (double ramification of the primary nerves.
This ramification is more distinct and more generally multiple, tbe
branches forking before reaching the borders and curving along them.
The leaf has, like those of the European species, a subbasilar marginil
veinlet, which follows the borders, and is united by nervilles in right
angle to tbe primary lateral nerves above.
Habitat. — Point of Rocks, Wm. Cldmm.
K 29. Rhus hembrakaoba, ip. nov.
Leaves small, membranaceons, thicktsh, oblong, obtnsely-pointed,
rounded or snbttuncate at base, irregularly coarsely dnplicato-dentate;
lateral veins open, the lowest decurving to the middle nerve, craspedo-
drome, more or less ramified.
LMQUBBKux.] FOSSIL PLANTS FROM POINT OF JSOCKS. 307
Of tbis species, there ia the point of a leaf, and another one nearly
entire, though somewhat lacerated, about two and a half centimeters
long, including the petiole (three millimeters), and one and a half
centimeters broad, oblong or Ungulate, with borders cut from the base
iu comparatively large, pointed teeth, either simple or with small pro-
tuberances on the back of the largest ones ; nervation craspedodrome,
the secondary veins entering the large teeth, and more or less irregu-
larly and obscurely dividing iu very thin branches, joined in the middle,
and forming a large, scarcely distinct areolation. By the form of the
leaves and the border-divisions, this species is comparable and closely
related to Rhus Pyrrhne^ Ung., as figured in Tert. Flor. Helv. of Heer
(PI. CXXYI, fig. 20), which has leaves, round truncate at the base, and
short- petioled, as in one of our specimens. Like Rhus Pyrrhw^ it is also
comparable to Rhu$ aramatiea Ait., a very common species of our pres-
ent fiora. This has also generally doubly dentate teeth, and, in southern
specimens, a thickish, membranaceous consistence.
Habitat. — Point of Rocks, Dr. F. V. Hayden.
'ISO. JUGLANS BHAMNOIDES, LSQX.
A small leaf of this species, which is not yet, however, definitively lim-
ited, as seen from the description in- Dr. F. V. Ha.yden's Report for 1871
(p. 294), and which may be identical with Juglans Leconteana^ Lsqx., and
Vomus acuminata^ Newby. Though it may be of the value of the species,
the leaf from Point of Rocks is identical in all its characters, even
in its size, with some of those found in the burned beds of red shales at
Black Butte.
Habitat. — ^Point of Rocks, Dr. F. V. Hay den.
The three following species have been sent also by M. Glebum from
near the Alkali stage-station, on the Sweetwater road, about thirty
miles north of Green River station of the Union Pacific Railroad. The
proprietor of the specimens did not himself visit the locality, but
obtained them from another party, who did not give any details on the
relative position of the beds where they were discovered. They repre-
sent three species, all new.
The character of the leaves, as also the presence of remains of Palms
at the same locality, seem to indicate about the same station as that of
Point of Rocks or Black Butte. They are described, therefore, as of the
same group.
T 1. ALNITES tTNBQUILATEBALIS, »p. nOV.
Leaves thin, variable in size, broadly oval or ovate-pointed, rounded
to a short petiole ; borders crenato-sernite; nervation pinnate; lateral
veins irregular in number and distance, curving in passing to the bor-
ders, at an angle of divergence of fifty to sixty degrees, and entering the
teeth by their ends or by small branchlets, wheu they pass under the
teeth and follow the borders.
These leaves vary in size from four to eight centimeters long and
from three to six centimeters broad, one of the sides measuring generally
one-fourth in width more than the other. The irregularity in the num-
ber of the veins is correspondingly great ; one of the leaves, the smallest
for example, has, on one side, five lateral veins, the lower much branched
outside, and on the other, ten, all simple. The largest of the leaves
of this species, which is represented by a number of specimens, is
related by form and nervation to Populus Xebrtditi, Wat., which Saporta
308 GEOLOGICAL SURVEY OF THE TERRITORIES.
conHiders as refenible to his Alnus oardiophylla. It is represented in the
Sezane Flora (Pl/XY, fig. 8). The general facies of the American leaves
is, however, different, the teeth l^ing broader and more obtase, the
nervation more distinctly pinnate, and the disposition of the veins to
enter the teeth by their extremity more marked; and compared to Alnus
cardiophyllaj it is especially different by the constant inequality of the
leaves. This last character and the irregularity of qervation are not of
frequent occurrence in the leaves of A {nte^. Alnus viridisau^A.serrtilatu
are, however, sometimes irregularly reined, and the ineqnality of the
sides is seen in a number of fossil species, AlniM cycladuvij Ung., especl*
ally A, sporadum^ Sap.
Habitat. — Alkali station, Wm. Clebum.
T 2. JUGLANS ALKALINA, Sp. flOV.
Leaves pinnately compound ; leaflets lanceolate, tapering npward to a
long acumen, either narrowed or rounded to a short petiole ; borders
crenulate; lateral veins distant, mostly alternate, parallel, separated by
short intermediate tertiary veins, curving in passing toward the bordeiB
at an open angle of divergence, and ascending high along them in fes-
toons ; nervilles in right angle to the veins, branching in the middle, and
forming, by subdivisions, irregularly quadrate or polygonal meshes.
This species is represented by four leaves, and its characters distinct.
It is comparable to Juglandites peramplus^ Sap., and Juglandites cemuuM,
Sap., both of the Sezane flora, partaking of some of the characters of
both. It is, however, still more intimately allied to Jvglans Bilinioa,
Heer (Flor. Tert. Helv., Ill, p. 90, PI. CXXX, figs. 5-19), from which it
merely differs by the position of the lateral veins at a more acute angle
of divergence following higher up along the borders, and by the thicker
and more numerous tertiary veins.
Habitat. — Alkali station, Wm. Clebum.
T 3. Carpites viburni, «/>. nav.
Seeds or nutlets cordate obtuse, five to seven millimeters long, three
or four millimeters broad, convex, grooved in the middle from the point
to the base, surrounded by a membranaceous pellicle, the remains of au
apparently fleshy outer envelope. They resem Lie seeds of a similar kind
which I have found in great quantity at Golden, and referred to the
genu9 VihuTmum. Their form is like that of the seeds of Ff6t(n»«im
Whympen, Heer (Spitz. Flor., p. 60, PI. XllI, figs. 22 and 27).
Habitat. — Alkali station, Wm. Cleburn.
NEW SPECIES OP TERTIARY FOSSIL PLANTS BRIEFLY
DESCRIBED.
The following-described species have been discovered since the publi-
cation of the last annual report of Dr. F. V. Hay den's Geological Sur>
vey of the Territories. They are represented by specimens sent from
different localities indicated, with each species, as well aa the name of
the discoverer. All these species have been figured for the second
volume of the Contributions to the Fossil Flora of the Western Terri-
tories.
/' 1. Sphebia bhytismoides, sp. nov.
The spots formed by this small fungus npon the bark of some stems
and Hie leaves of a Myrica are composed of circular perithecia, placed
ije»nuitifKi;x.l NEW SPECIES OP TEKTIABY FOSSIL PLANTS. 309
five or Rix in a circle, formiDg thus a small crenulate ring. The
peritbecia become connected sometimes, apparently by decomposition ;
tbey are, however, generally separated. The size of the spots varies
from one to two millimeters.
Habitat. — Black Batte, upon Caulinites Sparganioides.
'^ 2. Htpnum Haydenh, «p. nov.
Stem rigid, sparingly divided in nearly- opposite, short branches, in-
flated toward the top, or clab-shaped; leaves closely imbricated all
aroand, lanceolate-acaminate or sharply pointed, concave. Comparable
especially to Hypnum Bosciij Schwgr., an American species of the pres-
ent time.
Habitat. — South Park, near Castello Banch, Dr. F. V. Hayden.
^ 3. Lygodium Mabyinei, sp. nav.
A single leaflet of this fine species. It is simple, ligulate, obtuse,
(serrolate above, hastate at base; middle vein and veiulets distinct;
veins forking once or twice. Allied to the living Lygodium vennstum
which ranges from Mexico to Brazil.
Habitat. — ^Top of gypsum series, Grand Eagle j unction, A, B, Marvine.
4. IiYGODIUM DENTONI, «p. flOfJ.
Leaflets bi-tripartite, with short, obtuse divisions and broad sinuses,
broadly triangular, rapidly narrowed to a subcordate or subtruncate
base, entire, bi-trinerved from the base; primary nerves distinct, like
the veins, which are forked once or twice, and become very close along
the borders.
Habitat. — Green River group, near the mouth of White into Green
Biver, Frof, yfilliam DenUm.
•?
^-v
5. Gonioptebis pulghblla, f Heer.
An intermetliate form, represented by* mere fragments of pinnse and
separate pinnules. The shape of the pinnules united to the middle
refers it to 0. pulchella^ while by the less pointed leaflets and the nerva-
tion it represents G. Fischeri of the same author.
Habitat. — Golden, in sandstone, above coal.
6. Zamiostbobus T mibabilis, «p. nov.
This species, whose reference to Zamice is not positively ascertained,
is represented by a fragment, the half cross-section of a silicified cone,
about fourteen centimeters in diameter. The outer surface is marked
by the rhomboidal obtuse top of black seeds, or stony fruits, surrounded
by a white vtiscnlosocellular matter. In the cross-section of the cone,
these seeds, of an enlarged rhomboidal form, three to three and a half
centimeters long, six to eight millimeters broad, of the same size in
their whole length, or slightly narrowed to the base, appear fixed or
implanted into a zone of whitish, subpellucid mass of ceilulosovascu-
lar filaments. Under this ring of white matter, one centimeter thick,
comes the central part, or axis of the cone, represented by mixed frag-
ments of blackish opaque matter, agglutinated and amorphous. The
fruits, or seeds, are represented by a black, compact, opaque silex, pierced
in the length by large pores or ducts passing from the t4^p to the base
of the fruits. The intervals between them, nearly as large as the seeds,
are filled by the same whitish cellulosovascular matter which com-
poses the white zone wherein the ba^ of the fruits is embedded. The
310 GEOLOGICAL SURVEY OF THE TERRITORIES.
figure only of the specimen can give a good idea of tbis fragment of
cone. It is distantly comparable, lor the form and the disposition of its
surface-scars, to Androstrobus^ a genus established by 8cbimper for
some cylindrical cycadeous male cones, formed of imbricated scales bear-
ing sessile anthers on their lower surface. For the position of the froitSi
it has a distant relation to Zamiostrobus gibbusj Heuss., a cone which
shows, in its section, oblong seeds, in right angle to the axis, with their
tops appciiring at the outside surface. Both these cones are figured ia
Schimper's Yeget. Pal. (PI. LXXII, ligs. 1, 2, U, 15). There is, however,
a great difference in the very large size and in the characters of this
silicified strobile with those of a Zamia. It apparently represents a
peculiar genus of the Cycadinece,
Habitat. — Found loose around Golden, Dr, F. V. Hayden.
'T 7. Sequoia affinis, sp. nov.
Branches long, slender, pinnately branching; leaves short, oblong,
imbiicated and obtuse; or longer, lanceolate-acute, erect or slightly
retlexed ; brancblets bearing cones, open ; strobiles small, round-oval,
obtuse; scales large, rhomboidal, with entire borders, a central oval
mamilla, and wrinkles passing from it to the borders all around ; male
branches erect, with more acute and open leaves, resembling sterile
branches of Qlyptoatrobus Europeus^ with small, round catkins, covered
to the top by imbricated lanceolate leaves.
Tbis species, of which we have numerous and admirably well-preserved
S|)ecimeus, is much like Sequoia CouUicB^ Ueer, of the Bovey-Tracry flora,
differing, however, from it by the more obtuse point of the scale-like
leaves, by more acute and longer leaves of the sterile branches, by more
slender brancblets bearing cones at their ends, by proportionally larger,
more oval cones (not globular), by the indistinctness of a middle nerve
on the back of the leaves, which appear merely convex or inflated, etc.
The seeds are of the same size as those of ti» Coutsiw; they difter also
somewhat by a cordate base and a mere trace of middle m-rve near the
top, where it divides and passes on both sides, curving along the borders.
Habitat.— Middle Park, Dr. F. V. Hayden.
K 9. Sequoia aotjminata, sp. nov.
The form of the leaves is about the same as in Sequoia Xongifolia; they
are, however, generally shorter, narrower, less crowded upon the stems,
and especially distinct by the smooth surface of the leaves. In this
jspecies, the denudated branches are striate, while, in the former, they
bear the scars of the baseof the leaves. This difference, however, may be
merely the result of decortication in the specimens representing this last
species.
Habitat.— Black Butte.
T 10. Sequoia!, species.
Cones flattened, apparently long, linear-obtuse, marked at the surface by
shields of scales, (apophyses.) the only organs preserved. These are sepa-
rated from each other, not continuous nor imbricate, rhomboidal in outline,
With acute sides, and rounded top, bearing in the middle a round mamilla,
from which wrinkled lines are diverging to the borders. The 8i)ecimcn
represents two crushed cones, of which nothing can be seen but what is
described here.
Habitat.— Middle Park, Dr. F. V. Hayden.
i.x«Qi.^RBiJx.] NEW TERTIARY FOSSIL PLAKTS. 311
11 . Arundo reperta, 9p. nov.
Stem thick, articalated ; surface striated, marked witb roaod, obtase
knots, either placed ou the articolatious or here and there upoD the
stem, without normal distribution } ear of seeds crushed, representiug
lanceolate glumes, sharp-poioted and rounded at base, and ovate-lanceo-
l»te-acute seeds, truncate at the base, with the center elevated or con-
vex, apparently covered with a coating of hairs. The glume is longer
than the seeds, and nerved in the middle.
Habitat. — Green Biver, west of the station, Dr. F. V. Hayden,
12. Arundo obtusa, «p. nor.
Though the specimen is not as well preserved as that of the former
species, the characters of the organs which it represents are discernible,
and indicate a marked specific diiierence. The strisB or primary veins
of the small fragment of a brunch are thick, more distinct, and evidently
separated by four or five thinner secondary veins ; the glumes and pallets
are shorter, equally striate, without middle nerve, and the seed is much
shorter, broader, obtuse at one end, and truncate at the other. The
fragment which I consider a pallet is slightly emarginate or truncate at
the point
Habitat.— Golden, South Table Mountain.
-7
I <
13. Palm AOiTES Goldianits, «p. nor.
Species representing a large i'ragment of a flabellat^ leaf with five to
nine rays on each side, of a flat, narrow, linear rachis. Biiys averaging
one and a half centimeters broad, marked by deep, narrow farrows,
without costsB, joining the rachis in an acute angle of twenty degrees,
united to it by their whole undiminished base, without decurring along
it. Surface somewhat shining; substance thick ; primary veins distinct
at least in some places, where the epidermis is destroyed, two to two
and a half millimeters distant, separated by ten secondary veinlets, thin,
but often discernible to the naked eyes.
Ha bit AT. — Golden.
'Tl4. Sabal oommunis, 9p. nav.
Leaves of medium size, borne upon a nearly flat or merely convex
petiole, its top passing at the upper side into a short acuminate rachis,
while on the lower side it is cut liorizontuUy or nearly truncate; rays
not very numerous, the lowest in right angle to the rachis, not descend-
ing lower than its base, rapidly enlarging, carinately folded near the
point of attachment to the rachis, becoming mostly flat or scarcely
OS) rinate upward ; caiinie narrowly costate; primary veins broad, gen-
erally black when the epidermis is removed, one to two millimeters
apart; intermediate veins thin and numerous, avemging twelve in the
large intervals of two millimeters. This species is closely related to
Babat andegaviensis^ Schp. of the Eocene of Angers, France.
Habitat. — Golden, where it is common.
"y 15. Myrica Ludwigii, Schp.
Leaves of middle size, subcoriaceous, oblong or linear-lanceolate,
gradually tapering into a long entire acumen, distantly and deeply den-
tate along the borders ; middle nerve thick ; secondary veins suboppo-
site, open, parallel, curving in passing to the borders, camptodrome,
forking at the base of the teeth, the branches entering them, while the
top of the veins is curved along the borders.
Habitat. — Green lUver group, near mouth of White Biver, Prof. W.
Denton.
312 GEOLOaiCAL SURVEY OF THE TEBRITOBIES.
"^ 16. Mybiga insignis, sp. nov.
Leaf meinbraoaoeoas, large, narrowly-oval or oblonf? acaminate, prn-
uatelylobed ; lobes short, entire, tarned npward, triangalar-acate; lateral
ueina open, slightly carving in passing to the point of the lobes ; tertiary
veins nearly as thick as the secondary ones, forking ander the acote sinuaes
of the lobes, the branches ascending along the sides ; areolation large,
I)olygonal, formed b.v the anastomosis in the middle of the areas of
nervilles at right angle to the veins. There are of this beantifQl apeeies
two fragments of leaves, indicating the average size of ten ceotimeterB
long and four centimeters broad. The point, as in the former species, is
entire, and still more rapidly and acutely acuminate; and the lobes,
alternate, short, equal and similar, give to this species a beaatifol ap-
' pearance.
Habitat. — Middle Park, Dr. F. F. Hayden.
^ \ 17. Mtbioa f Lessigiana, sp. not?.
This species is represented by nearly the half of the leaf, enormous,
at leastif it belongs to this genus. Leaf linear, oblong in outline, deeply
lobed ; lobes ojiposite, ovate-lanceolate, obtusely pointed, at an open
angle of divergence, entire, joined at a short distance of the thick mid-
dle nerve in obtuse sinuses ; lateral veins thick, subopposite on an
open angle of divergence, asceridiug to the point of the lobes, rami-
fied from the middle npward in branches curving to and along the bor-
ders ; tertiary veins, variable in thickness, relative position and direction,
some forking under the sinuses, and passing upon both sides of it;
others traversing the large intervals betweetl the b9>se of the secondary
veins and the borders of the lobes, and following the borders in multiple
festoons; areolation of the same character as in the former species, the
large areolse, however, being subdivided in very small meshes of the
same character. •
This magnificent leaf seems of a pellucid texture, though thick ; at
least, all the details of areolation and nervation are distinctly perceiv-
able in black upon the chestnut-color of the leaf. Though the fragment
does not represent one-half of the leaf, the terminal leaflet being de-
stroyed, and the base also, still it is twenty-three centimeters long and
eighteen centimeters broad, each lobe being nine to ten centimeters
long from the middle nerve to the pomt^ and seven and a half centime-
ters broad between the sinuses. It is doubtful if this leaf represents, as
the former, a species of the section of the CampUmia, It resembles
Camptonia grandifolia^ CTDg-j which was till now considered as the giant
representative of the section, but whose leaf is scarcely half as large as
this. The nervation and areolation of this leaf are of the 8amecha^
acter as that of Myrica^ identical, indeed, to that of 3/. Matheraniane Sap.,
Et. II, 2y p. 93, T. v.. Fig. 7, whose lobes are also of the same form. It
is much larger, however, too large it seems for a Myrica. By the forin
of the leaf it is comparable to Ardlia multifida Sas, Et. 1, 1, T. Xli, f.
1 and 1^, and also but more distantly to Ciissaniapolydrys Uug., Flora
von Euboea, p. 47, T XVII, f. L
Habitat. — Found in connection with abed of lignite west of Denver,
Colo., aud kindly communicated by Mr. TF. H. Lessig^ who discovered
it, aud had the specimen framed in a bedding of plaster.
\' 13. Betula Vogdesii, sp. nov.
Leaves small, ovate, acutely-pointed, rounded, and narrowed to the
petiole, minutely serrulate, penniuerve, lateral veins distant, opposite ator
UBM)umux.j NEW TEBTIAEY FOSSIL PLANTS. 813
near the base, simple or rarely brancbiDg, passing up in an angle of
divergence of thirty to thirty-five degrees, nearly straight to the bor-
ders, craspedodrome ; details of areolation obsolete.
Habitat.— Near Fort Fetterman, in connection with a profusion of
remains of Tmxodium distiehumj Ideutenaait Vogdes.
^ 19. CASTANEA INTEBHEDIA, 4^. nOf.
Leaves proportionally long and narrow, linear-lanceolate pointed,
narrowed to the base ; borders equally and sharply dentate ; teeth acu-
minate, turned upward ; areolation and nervation similar to that of
Castanea Veaca. By its character it is intermediate between Castanea
JJngeri of the Miocene and 0. vesca*
Habitat. — Middle Park, Dr. F. V. Hayden. ^
~ 20. CARPINUS aBANBIB, Uug.
This species, so common in the Miocene of Europe, is represented ia
oar flora by a number of leaves identical in all the characters.
Habitat. — Near Florissant, South Park, Dr. F. F. Hayden.
T 21. QUEBCUS Haidingebi, Ett
Leaf ovate-lanceolate, narrowed to the base (point broken) ; borders
obtusely crenatoserrate ; lateral veins numerous, close, on an angle of
divergence of forty to forty-five degrees, rarely branching, camptodrome
and craspedodrome. The leaf appears to.be tapering to a point. It is
upon coarse sandstone, and the details of areolation are totally oblit-
erated. By its form, the divisions of the borders, and the nervation, it
agrees with the characters of the species, except that in this leaf the mid-
dle nerve is not thick, as described by Heer.
Habitat.— Green River, Dr. F. V. Haydei^
'^ 22. Planeba UNaEBi, Ett.
Leaves short-petioled, ovate, acuminate, narrowed to the base, simply,
coarsely serrate Irom the middle upward } secondary veins nine pairs,
passing up to the point of the teeth in an acute angle of divergence. This
form, though represented by one leaf only, is in entire concordance of
characters with those of this species widely distributed in the Miocene of
Surope.
Habitat.— South Park, Capt. Ed. Berthaud.
T >
23. Ficus ovALis, 8p. nov .
The only leaf repeseuting this species is coriaceous, oval, entire, nar-
rowing in a curve to a long thick or flat broad petiole, grooved in the
middle penninerv; lateral vein alternate, camptodrome, curving along
the borders in fiestoous ; tertiary veins short } areolation obsolete. The
upper part of the leaf is broken.
Habitat.— Pleasant Park, Plum Creek, Dr, F. V. Hayden.
I 24. Picus PSEUDO-popuLUS, sp. nav.
Jjeaves oval-pointed, narrowed to the petiole, entire, three^erved from
the top of the petiole; lateral veins at an acute angle of divergence,
like the secondary veins, two or three pairs, the lower of which is at a
great distance from the primary ones, camptodrome; nervilles distinct,
in right angle to the midrib, crossed by oblique brauchlets, forming a
large equilateral or polygonal areolation. A remarkal>id species,
314 QEOLOGICAL SUBVET OF THE TEBRITOBIES.
resembling a Cinfiamomum by the nervation of its leaves and a Zizjfphru
by the form.
Habitat. — Evanston, Dr. F. V. Hayden. .
>•! -
T 25, Ficus Wyomingiana, ap. nov.
May be a variety of the former, resembliog it closely by the form of
the entire, long-petioled leaf. The difiterence is marked, however, by
the total absence of secondary veins; the middle nerve bein^ joined
to the lateral ones by strong nervilles in right angle.
Habitat. — West of Green Biver station, Dr. F. V. Haydenu
^ 26. Diosp YEOS ! FiGOiDE A, «p. nov.
Leaf ovate, narrowed to a point (broken), rounded to the petiole,
thickish, entire, pinnately- nerved; midrib thick, deeply marked, as also
the secondary veins, parallel, at an acute angle of divergence, all doubly
camptodrome ; fibrillaB thick, nearly in right angle to the veins, divided
in the middle; areolation square or polygonal ; surface rough. The
generic relation of these leaves is not satisfactorily fixed.
Habitat.— Black Butte.
^ 27. Viburnum platanoides, sp. nov.
This species essentially differs from Viburnum marginodum by the less
numerous, more open, lateral veins, whose branches are more curved in
passing up to the borders, and especially by the enlarged truncate or
snbiruucate base of the leaves. The direction of the veins along the
lower branches of the lateral veins is the same, and the borders are den-
tate in the same manner, though not black -margined as in V. margin-
atum.
Habitat. — Black Butte, mixed with Saurian bones, and as abun-
dant in that bed as is its congener, in the shale above the main coal
of the same locality.
T 28. CiSSUS PABOTTIJSFOLIA, Sp. nOV.
Leaves ovate-subcordate or narrowed to tne base, gradually and ob-
tusely pointed, undulato-crenate, threenerved from the top of the peti-
ole or from a little above the border- base ; lower secondary veins at a
distance from the primary ones, which are much divided ; all the branches,
like the secondary veins, craspedodrome ; nervilles strong, in right angle
to the veins; areolation small, square, b^ subdivision of veinlets.
The species is represented by a few leaves, one of them, fragmentaiy,
has a cordate, unequal base, and may belong to a different species.
Habitat. — Green Biver, west of the station, Dr. F. V. Sayden.
K 29. Bhamnus Bossmasslebi f , Heer.
Leaves oblong-obovate, obtusely pointed, entire, narrowed to the base,
penninerve ; secondary veins close, parallel, passing to the borders nearly
straight and curving along them in festoons. These leaves are small;
one only is preserved entire; their speciQc relation is not. fixed.
Habitat.— Black Butte.
^ 30. Phaseolites juglandinus !, Heer.
Leaflets of an apparently compound leaf, oval-oblong, obtusely pointed,
rounded to a short petiole, entire, subcoriaceous, penninerve; lateral
veins parallel, distinctly camptodrome, and following the borders in fes-
toons ; ultimate areolation small, irregularly quadrate.
7'
1
UBQURREux.] NEW TERTIARY FOSSIL PLANTS. 315
The species may be different from tbe Earopean one bearing tbis
name, but it appears to differ only by more open secondary veins.
Habitat. — Green Kiver group, near month of White Eiver, Prof.
Wm, Denton.
31. liEGUHlNOSITES ALTERNANS, «p* noV,
Leaflet lanceolate, narrowed to the sessile base (point broken), appa-
rently tapering and acute; borders entire; secondary veins close, nu-
merous, fifteen pairs in a space of two and a half centimeters, with in-
termediate shorter tertiary veins anastomosing by crossing veiulets;
areolation obsolete. This leaf is comparable to a Dalhergia or a Podo-
gonium by its nervation ; its form, especially the narrowed base, is com-
parable to Cassia.
Habitat. — Near month of White Eiver, Prof. W. Denton.
32. Sapindus Dentoni, sp. nov.
Xieaves lanceolote, gradually narrowed to a long acnmen, nnequilat-
eral and rounded at base to a short petiole, entire or slightly undulate,
thick ; secondary veins close, parallel, diverging forty to fifty degrees,
thick, straight to the borders, where they abruptly curve, and which they
closely follow.
Species allied to Sapindus falcifoliuSy Heer, but remarkably distinct
from this and other congeners by tbe thick, close, lateral veins straight
to the borders, where they curve so abruptly that they appear at first
sight as craspedodrome. The areolation is of the same character tis
that of S. falcifolius.
Habitat. — Green Eiver group, near mouth of White Eiver, Prof. W.
Denton.
33. LOMATIA MIGROPHTLLA, sp. noV.
Leaves very small, thick, coriaceous, linear-lanceolate, gradually nar-
rowed to a point, and in the same degree to the base ; secondary veins
simple, thin, in an open angle of divergence, connected to a marginal
vein. We have two leaves of this fine species. It is comparable to
Lomatiafirma^ Heer, of the Baltic flora, but very small and thick; the
snrface mostly covered by a coating of coaly matter.
Habitat. — Same locality as the former, Prof W. Denton.
A large number of fruits and seeds, considered under the name of
Palmacites^ CatpoliteSy etc., have been figured i'or the Lignitic Flora. As
the characters of these organs cannot be represented by mere description,
they are not mentioned in this short synopsis.
A REVIEW OF THE CRETACEOUS FLORA OF NORTH AMERICA.
§1.— GENERAL BEMABKS.
The formation known ander the name of Dakota group is positively
determined as Cretaceous by the animal-remains profusely embedded
into the strata overlying it. This fact has been repeatedly and cleari;
exposed in the former reports of Dr. F. V. Hayden. As this formatioo
rests immediately upon thick limestone beds of Permian age, its Aon,
which is mostly represented by dicotyledonous leaves, has apparently no
ancestors in this country. In Enro[)e, the dicotyledonous plants of tb»
Cretaceous epoch are scarcely known, or, at least, they have not yet
been satisfactorily studied and described. The more recent and impor-
tant publication on the subject refers to the Cretaceous of Greenland,
and exposes the specific characters of a proportionally large namber of
Cryptogams and Gymnosperms, Ferns, Conifers, Cycads, with few Dicoty-
ledonous. Three of these only are represented in the flora of the Dakota
group. There is, therefore, from antecedents or from contemporaneoas
floras, no points of comparison to which the character of the plants of this
group might be referred. For analogies, we have to look to spe-
cies described from more recent epochs. And, in these researches,
the paleontologist is met with another kind of difficulty. The straU
where the dicotyledonous leaves are found in Kansas, Nebraska, Dakota,
&c., are separated from the Lignitic-Tertiary formations by a few tboa-
sand feet of measures, mostly shale and sandstone, all of marine origin,
with animal fossil-remains denoting an uninterrupted series of Creta-
ceous types. These strata are generally overlaid by heavy beach-sand-
stone locally interspersed with fucoldal remains, extremely abundant in
some places, or with a mass of crushed, half-pulverized fragmentsof land-
plants. Over this, the Lignite beds come to view, with their accom-
panying shales and sandstones, wherein vegetable remains are found
sometimes in profusion and in a beautiful state of preservation. Here,
then, we should expect to recognize forms of leaves or species, if not
identical with those of the Dakota group, at least showing, as probsble
offsprings, some affinity of characters with them. This as yet is not
the case. The typical forms of leaves of the iN'orth American Creta-
ceous are not at all repeated in the Lower Lignitic flora of the Rocky
Mountains, not more than they are in the Lower Eocene of Earope.
With the exception, however, of the peculiar type of oak and chestnat,
Bryaphyllumy which originates in the Middle Cretaceous of both con-
tinents, is recognized in species of the Lower Eocene of France, Sezaud
and Gelinden, as in that of Point of Bocks, in Wyoming, and leaving
some of its representatives in all the geological series, passes to tbd
flora of our time. Some few more leaves of the Dakot>a group have a
relation to species of Evanston, especially to- those of Miocene of Car-
bon, in the same proportion, about, as they have to Miocene species oi
Europe ; more still are closely allied to species of the Pliocene of Oali*
I'omia ; but the analogies become far more evident and marked, also, b;
316
t.Ka<iXj:BREUx-] REVIEW OP CRETACEOUS FLORA* 817
nnmeroas points of similarity, in the present vegetation of 'the
.^trlnntic slope of North America.
"Xljis absence of related forms in the nearest geological series of the
Ojnetaceous, the re-appearance, also, of Cretaceous types in more recent
fox-matlons, and especially at this time, are perplexing, indeed, to 1 he
qoerist, surrounding the study of this flora with a great deal of nncer-
'ta.inty and of difficulty. Who can believe that the dicotyledonous plants,
^^irliich were destined to take such an immense predominance in the vege-
t:at^ion of the world, were, from the beginning, the same as they are now ?
S^ow suppose that, after their exclusion from the floras of long geo-
log^icar epochs, a number of them have re-appeared anew, with their
original characters? This would seem an anomaly, in contradiction to
'wliat is known, or, rather, generally admitted in regard to the succession,
'tlie DQultiplication, and the improvement of types, in following the ascend-
ii3^ grade of the vegetable reign in its development. Do we not miS'
take in recording, as evident and close points of affinity, what may be
mere illusional appearances I Questions of this kind give to the study
of the North American Cretaceous flora a higher degree of importance,
'but, at the same time, force the paleontologist, who is trying to decipher
tlie hieroglyphic records of the old floras, to pursue his researches with
tiie greatest caution, reviewing again and again the forms which lie con-
siders as specific, comparing them from as large a number of specimens
as may be obtainable, especially studying their relations with the veg-
etable contemporaneous types recognized in the same formations, or in
those of another country. This renders the acquisition and the study of
new materials constantly desirable, and, therefore, subject the conclu-
sions arrived at to possible modifications. For this reason, the first
volume of the Cretaceous flora of the Dakota group should be considered
as an incomplete memorial, to which successive supplements have to be
added by every one who, engaged in paleontological I'esearches, is in
po8ition to get specimens of fossil plants from this group. The present
review is one of these supplements, demanded tor the reasons alluded
above; first, by the discoveries in the Cretaceous formations of new and
important materials, modifying, by their characters, generic divisions
fixed from insufficient specimens, or adding new species or new types to
those which were already knoWu ; and, secondly, by the critical notices
of learned friends, at home and abroad, who, sensible to the importance
of the data ofllerea to science by the first exposition of the flora of the
Dakota group, have urged me to pursue the work merely begun, and
to bring forth, without delay, the results obtained by these new re*
searches.
There is, however, still another and more forcible inducement to re-
view successively the data procured by new researches and discoveries,
in addition to our knowledge of the North American Cretaceous flora.
It is the insufficiency of the materials obtainable fortbecomparison and the
determination of specimensof fossil plantsin thiscountry. Messrs* Debey
and Ettlngbansen began the study of the Cretaceous flora of Belgium al-
ready in 1843. After spendinga few yearsin exploring the Cretaceous for-
mation in its geological and stratigraphical distribution and in collecting
specimens, having, as they supposed, about three hundred species to an-
alyze, they published, in 1848, an abridged synopsis or general review of
the Cretaceous flora of Belgium, describing then only a new genus of
Conifers, and a few species referable to it.* In 1849 they still published, as
* Ubersicht der unveltliobeD Pflanzenreete dcs Kreidegcbii^es tiberbaupt, nnd der
Aacbener Kreidescbichten im Besonderen, in Verb, des nat. VereiDee d. preos. RheiD-
landd, 1848.
31ft GEOLOGICAL SURVEY OP THE TERRITORIES.
eA^deDce of the progress of their researches, a catalogue, names only, of
seventy species of their Belgian Cretaceous plants. But after they had
enlarged their collection of specimens, and pursued their work of compar-
isoD, they were soon called to review their first determinations and to
acknowledge that very few of their former specifications could be pre-
served, as they had to unite in one species a. number of forms which were
first considered as different, or to separate some others which they had
formerly admitted as identical. In 1850 the great herbarium of the
Botanical Garden of London was opened to them, and they had free ac-
cess to the immense materials, especially exotic species of plants of the
present time, which they wished to have for comparing the vegetable
forms of the Cretaceous. In 1851 the celebrated authors published an-
other short genial review of the Cretaceous flora of Maestrich. These
were merely introductory memoirs to the work which they had under-
taken, and for which they acknowledge the assistance received, not only
by direct communications of the greatest botanists and paleontologists
of the time, Brongniart, Decaisne, Hooker, &c., but also by the free use
of the largest botanical and paleontological collections of Europe, and
of scientific libraries, where they could study, from its origin, the lit-
erature referable to vegetable paleontology } all the papers, even the
most unimportant, which have been published on the subject. It was
only, in 1859, and after nearly fifteen years of stpd}', that the first
and second parts of their work were published. The first, concerning the
Thallophytes, describes and represent, in three plates, eighteen species
of Fucoids, or marine plants, four species of Fungi, and one Lichen.
The second part, on the Acrobrise, describes, with figures, forty-one spe-
cies of' Ferns, and two species of doubtful relation to this family.
Since then nothing more of this work has been published, and we know
the dicotyledonous leaves, whose remains are said to abound in the Bel-
gian Cretaceous formation, merely by some generalities related to their
classification and a few generic names.
The work of the European authors is certainly of the highest scien-
tific order, and might be taken as a model to be followed for proceeding
in paleontological researches in our country. But who could work ten
to fifteen years in preparing the publication of a report, when in his re-
searches a naturalist does not find any materials for comparison. We
have, as yet, no valuable collections in vegetable paleontology, and it is
especially because the first materials have to be carefully prepared for
institutions of this kind, that the paleontologist is called to review and
correct his determinations as fast as new materials are prepared for ex-
amination.
The plants of the Dakota group, as known mostly by detached
leaves, are striking by the beauty, the elegance, the variety of their
forms, and of their size. In all this they are fully comparable to those
of any geological epoch as well as to those of our time. From entirely
developed leaves, less than one inch in size, they show all the gradations
of size to one foot, even to one foot and one-half in diameter. The
multiplicity of forms recognized for a single species is quite as marked
as it might be upon any tree of our forests. And to expose the admira-
ble elegance of their forms, it suffices to say that, at fii-st sight, they
forcibly recall those of the most admired species of our time: the tulip-
tree, the magnolia, the sassafras, the sweet-gum, the plane-tree, the
beach, the aralia, &c. The leaves of Protophyllum Stemhtrgii have the
size and the facies of those of the catalpa, one of our finest ornamental
trees. Those of Menispermites obtusilobaj of Protogpermum quadratum,
represent in the same manner some of the rarest shrubs, Metii^permum^
iJKSQUEBEiix] EEVIEW OP CRETACEOUS FLORA. ♦SIS
JS^erdinandia^ &g., carefally raised in conservatories for the graoe-
ful forms of their leaves or the richness of their vegetation. It is
indeed the first impression received from the beauty of forms of the
leaves of the North American Oretaceoas, and the evident likeness
of their facies to that of the finest vegetable types of our time as we see
t.bem around as, which strikes the paleontologist and may lead hiui into
error, in forcing upon the mind the belief of a typical identity where,
possibly, there may be a mere likeness of outlines, a casual similarity
of forms in the leaves. For, really, when we enter into a more detailed
analysis of these Cretaceous leaves, we are by and by forcibly impressed
by the strangeness of the characters of some of them, which seem at
variance with any of those recognized anywhere in the floras of our
time, and unobserved also in those of the geological intermediate
periods. Not less surprised are we to see united in a single leaf, or
species, characters which are now generally found separated in far dis-
tant families of plants. The leaves of Eremophyllum^ so striking by
the peculiar appendages of their borders; those of Anomopliyllum^ refer-
able to planes by one half, to oaks by the other; those of Vlatanvs
obtusHoba, half Acer^ &c., are of this kind. On another side, the charac-
ters of some of the Cretaceous species are sometimes of such a transient
or indefinite order that it is scarcely possible to take hold of them and
to expose them with a degree of reliance. At first sight they seem
very distinct, but, in comparing a number of specimens, the differences
dwindle by unmistakable transit^ions, and disappear. In other leaves,
on the contrary, visibly identical by their outlines, the nervation is so
different that they are forcibly separated and referred to far distant
generic divisions. Hence, this flora does not leave any satisfaction,
any rest, to the mind. Even the most clearly defined types become
doubtful in regard to their integrity when we see others, which at first
were recognized as positively fixed, manifesting instability and pointing
to diversity of relations by the discovery of new specimens. The
leaves considered first as Sassafras seemed evidently referable to this
genus; but when leaves of the same type were found with dentate
borders, though bearing besides all the characters of a genus which
belongs to the LaurinecBj a family where, as yet, no representative has
been found with dentate borders of leaves ; when others were obtained
with subdivision of the lower lobes in two or three, thus showing the
palmate shape of Aralia leaves, the confidence in the value of the char-
acters at first recognized had to be abandoned.
This revision l)ears, therefore, on the degree of relation, or of generic
identity, which may exist between the leaves of the Dakota group and
species of plants living at our time in this country or described from
intermediate geological periods; on the degree of persistence in the
characters which have been, or should be, considered as specific in the
determination of these leaves ; on the essential types of the Cretaceous
flora considered as original, derived, or ancestors. These questions
cannot be examined in the order where they are presented above ; but
they may be touched upon, as far as opportunity is offered, in remark-
ing upon the different vegetable groups represented in this flora.
It is remarkable that though the Dakota group formation is recog-
nized as marine by the presence of marine fossil mollusks, no remains
of marine plants have been to this time found in any part of its strata.
Divers reasons may be suggested in explanation of this fact ; the coarse-
ness of the matrix, for example, wherein the vegetable fragments were
imbedded, and where mere cellular and soft plants could not be pre-
served. The fossilization of the leaves in the red ferruginous shale of
320 . GEOLOGICAL SURVEY OF THE TERRITORIES.
the Dakota group is not a true petrification. The forms or casts onlr
are left after the total destraction of the sabstance. This may explain
how most of the leaves which have been obtained trom this gronp of the
Gretaceoas are of a coarse, thick, corinceons texture. The delicate or-
gans of plants, like thin leaves or sea-weeds, may therefore have been
totally destroyed. If it is so, we know from this flora a part only, the
one which is represented by leaves of a hard tissue and by somelfraits
and stems. At different places and horizons of the forqsation. especially
near the upper part and at the base of the measures, one finds thin beds
of black, plastic, soft clay, where reuiains of plants could be preserved
in their integrity even with the epidermis of the leaves.. A sing^Ie leaf
has been found of that kind near Sioux City; it is referable to one of
the species most commonly represented in the red shale, and therefore
does not afford any point of comparison. The other deposits of clay
have been found either barren of vegetable remains of any kind, or,
also near Sioux City, mixed with decomposed, undeterminable frag-
ments, especially of leaves of Conifers and of rootlets of water-plants,
As it is the case in the red shales of the other formation to which this one
has been compared — the Upper Devonian, the Lower Permian • — thin
layers of coal or coaly matter have been deposited here and there in the
80 called sandstones of the Dakota group. They are no coal-beds, bow-
ever, but mere attempts or premises, and preparatian also, of a future
Carboniferous formation. In the strata related as synchronous to the
Dakota group, in Canada, Kew Mexioo, New Jersey, &c., no workable
coal-bed has been discovered till now. Some, which may be compared
to the subconglomerate coal-beds of the Carboniferous, have been appa-
rently formed near the end of the Cretaceous epoch. As yet, their fossil
flora is unknown. In connection with the thin layers of coaly matter in
the shale of the Dakota group, no specimen of fossil plants has been
discovered till now.
Toward the end of the period of the Dakota group and in the upper
beds of the formation a rapid succession in the elements of the com-
pounds, mixed in various ways, in the size of the dSbris^ etc, indicates a
new influence, the introduction of deep marine water by slow submer-
sion or subsidence of the land. It is after this, or in the Niobrara gronp.
that the only species of marine plant described in the Cretaceous Hora
has been found. This Zonarites digitattutji though similar in its char-
acter to the si»ecies published under this name by Brongniart and Geinitz,
has its relation contradicted by the great difference between the geolog-
ical periods where the remains have l>een found in Europe and in
America, and still more perhaps by the difficulty of identification of ma-
rine plants whose characters are represented merely by a vague likeness
of outlines. It would have been advisable, perhaps, to leave out without
description a vegetable of that kind, not even referable to the Dakota
group, and to leave also without even a mention mere fragments like
those described as Ligodium trichomanoidesy Abielites Haydeniij Flahei-
laria minimaj etc., whose characters and relation are too vaguely indi-
cated. .But as the Cretaceous plants of this and other countries are
scarcely known, it seemed proper to represent by drawing all the dis-
cernible fragments, leaving to time an opportunity of confirming or
refuting by better specimens the first determination. Even small frag-
ments may become valuable as complement of other specimens which,
fragmentary also, may be defined by those which have been published
before, and which, for the same reason of defectiveness, shoold be left
• Cretaceous flora iu Dr. F. V. Uaydeo's Report, vol. vi, pp. 26, 27.
t Gretaceoas Flora, p. 44, PL I, Fig. 1.
uiMQUKRKux.J REVIEW OP CRETACEOUS FLORA. 321
aside as rabbish. Anemidium Schimperi^ Sphenopteris grenillioides^ efc.,*
of the Cretaceous Arctic flora of Heer, are not more subject to satisfac-
tory determiuatiou tban^ Lygodium trichomanoides or Fterophyllum Hay-
€l^nii. Moreover, this last species, thougb imperfectly represented, indi-
cates a point of relation between the Dakota group flora and that of the
Cretaceous {Quadersandstein) of the Hartz Mountains in Germany.
X^Yagments of this kind are, therefore, doubly interesting by botanical
and geological affinities.
Before entering farther into the discussion and comparison of generic
and specific types of the North American Cretaceous flora and ot their
relation with vegetable forms described from Cretaceous formation of
other countries, I have to add a few remarks more on the third volume
of the Arctic flora of Heer, which was in publication at the same time
as that of the flora of the Dakota group, and of which I could give
only a short mention (p. 40), from a general synopsis formerly published
by the celebrated author. The Cretaceous flora of Greenland, which
constitutes the essential part of this third volume,* is in two parts.
The first describes beventy-five species from four different localities of
the north side of the peninsula of Noursoak, North Greenland, repre-
senting a lower stage of the Cretaceous. Of these, thirty-eight belong
to Ferns,t four to Lycopods and Equiseta, eight to CicadesB, sev-
enteen to Conifers, six to Monocotyledons, and one to Dicotyledons.
This flora is, therefore, composed of fifty-six per cent, of Acrogcns,
Ferns, Lycopods, and Equiseta; twelve per cent, of Cycadese; twenty-
two per cent, of Conifers ; eight i>er cent, of Monocotyledons ; and one
j>er cent, of Dicotyledons. In the Ferns, the genera Aspleniumy
Pecopteris^ Oleickeniay are predominant, this last genus especially, which
is represented by thirteen species. In the Cicadese, the Zamites, five
8|>ecies ; in the Conifers, the Sequoia and PinuSy the firat with five spe-
cies, the second with four.
The second part of the Greenland Cretaceous flora describes remains
of plants, especially found in the southern part of the same peninsula.
Considered as Upper Cretaceous by the author, it has in sixty-two
species, thirteen Ferns, two Cycadese, ten Conifers, three Mono-
cotyledons, and thirty- four Dicot.\ledons. The relative proportion of
these plants is therefore far different, as here, fifty five per cent, are
Dicotyledons. In regard to their generic distribution the predominance
is marked, in the Ferns by Pecopteria and Oleichenia^ in the Coniters by
Sequoia and PinuSy and by PopuluSy ProteoideSy ChondrapkyUum^ and
Magnoliay in the Dicotyledons. And in considering the general character
of the land vegetation of North Greenland, at the Cretaceous epoch, and
as far as it is known for the present by counting together the species of
both stations, we find it represented by a percentage of thirty-seven for
the Ferns, three for the Lycopodiacese and Equisetace®, eight lor the
Cycadese, nineteen for the Conifers, six and a half for the Monocotyle-
dons, and twenty five for the Dicotyledons, which therefore represent
only one-fourth of the whole.
The first exposition of the Dakota group flora shows four species of
Ferns and six species of Conifers only. To this small number we have
* A number of the Crotaceoas plants of Cape Staratsohin, Spitzber^, are also described
in this work. They represent five Ferns, one Eqoisetam, nine Conifera, and one Mono-
cotyledon, or sixteen species. The predominance of Conifers is remarkable as wen
as the absence of CycadesD and of Dicotyledons. Of these species, three Ferns and
three Conifers are identified with the lower Greenland flora, and five Conifers with the
apper, indicating an equal relation to both or an intermediate geoloji^ical station.
t By a misprint in the ibove exposition given in Cret. Flora, p. 40, the word FuooidB
is written for Ferns.
21 H
322 GEOLOGICAL SURVET OP THE TEBRITORIES.
added in this review one species of Oleicherda and five species of Conifers.
The specific value of some of the vegetable remains referable to this last
familj is, however, donbtfol, especially for those which are represented
by cones only, Ahietites Embstinod^ Sequoia formosa^ Sequoia JReick-
enhcuihi, and the fragments described as Inol^nSj all which, however,
though uncertain their specific or generic relation may be, are evideDtij
representatives of some species of Goniferis. Tbe fragments referable
to tbis group are of a difficult determination ; for the organs represented
upon the coarse shale or hard ferruginous sandstone of tbe formation,
merely expose some outlines of their forms by the same kind of fossili-
zation or molding, remarked already for the leaves. We do not find,
therefore, any flattened cones with the scales, any flattened branches with
leaves, but impressions only, more or less deeply carved into the
stone, the cones even passing through the shales and showing the space
originally occupied, as a mere cylindrical hollow, around which the forms
of the scales are more or less clearly engraved. The numerous leaves of
PintM spread upon the surface have dug in the same way and bv their
hard substance, narrow linear channels, representing the back of
these leaves, with an indistinct midrib, and the branchlets of Sequoia
also are seen as longitudinal grooves, bearing on both sides tbe same
impressed form of their leaves. This cannot be considered a very dis-
tinct representation of characters, the minute details desirable for an
exact determination being more or less obsolete.
Among the specimens recently examined, a fragment has been foood
referable to PhyUoeladus ; the presence of this genus in the Cretaceous
flora is thus sufficiently ascertiuned. We may, therefore, record as
recognized in the flora of the Dakota group, for the Ferns, the genera
Lygodium^ SphenopteriSy Hymenophyllum^ and Oleichenia^ tbe three first
by each one species, the last by two ; and in the Conifers, Sequoia^
by three species ; Finus^ by one, and Phyllodadus by one, leaving^ oal
as of uncertain generic relation with the cones mentioned above,
Glypto8trobti8 (t)gra4^llimusy whiGh is i)evhsip8identi^ab\e with Sequoia
condita, or with FreneliteSy and Oeinitzia (f ), known merely by the im-
pressions of some detached scales. To this should be added Araucaria
spatulata^ described in extinct floras of North America by Dr. Kew>
berry, from Nebraska specimens.
A fine plant, doubtfully described with the Ferns in Cretaceona
Flora, p. 48, Plate XXIX, figs. 1-4, under the name of Todea (f )
saportaneaj has to be eliminated from this family. For, though the
shape of the leaflets, their mode of union to the rachis, the position
of parallel equal branches are, by similarity, comparable to leaflets and
to divisions of fronds of ferns, tbe areolation of the leaves, which has l>ei*a
studied from better specimens and figured here again, PI. VI, fig. 2,
more positively relates these vegetable fragments to a peculiar section
of the Proiedceoe or to Lo^natia^ a genus especially represented in Ans>
tralian Islands and on the southwestern coast of South America, Chili,
and Peru. For this separation I readily submit to the opinions of
learned friendly critics. But I cannot consider the glumaceous leaf and
tubercle described as Phragmites cretaceous in Cret. Fi., p. 55, PL I,
figs. 13, 14, and PI. XXIX, fig. 7, a« a species of Draccena or Yucoa^ &c
The tubercle represented (fig. 13) is really similar to organs of the same
kind found attached to Bhizomas and to stems of fossil Phragmites and
Arundo. And for confirmation of the warranted reference of the^e
fragments, we have now in Arundo greenlandiea^ Heer. Fl. Arct, VIII,
p. 104, PI. XXVIII, figs. 8-11, leaves which, though narrower, have the
same form and the same characters of nervations as those of the Dakota
UMQUKBEux.] REVIEW OP CRETACEOUS FLORA. 323
^onp. In the Kansas specimens only the epidermis of the leaf is
destroyed at a few places where the veiolets become perceptible. Gen-
erally, however, as in the specimens of GreenlaDd, the primary veius
only can be seen.
Of the fragments donbtfally referred to Flabdlaria t and described
as F. minima^ Gret. FL, p. 56, PI. XXX, fig. 19, nothing more has been
discovered in regard to their relation, which has to be considered as
nnkoown as yet. The same may be said of the peculiar vegetable form
described in Gret. FL, PI. 1, fig. 6, as Pterophyllumf Haydenii, which
waa supposed to represent some kind of Cieadeoe. It difters from any
species known of this family by the broad stem and short leaves, nar-
rowed to the point of attachment, and from these characters Professor
Heer thinks it reterable to Gonifers.
!Now, counting the leaf described as Diosooreaf cretaceay whose generic
reference may be donbted, but which evidently represent a species of
the DioscorecB or a monocotyledonous, and also the fragments referable to
Conifers in the description, we have to this time, in the flora of the Da-
kota group,and exclusively of the dicotyledonous, sixteen specific forms,
representing the cryptogamous acrogens by five Ferns, the phoBuogamons
gymnosperms by nine Gonifers, and the monocotyledonous by one glu-
maceons and one petaloid species.
The first dicotyledonous leaves described in the Gretaceous Flora,
under the name of Liquidambar integrifolium^ have been considered by
some authors as uncertain in regard to their generic relation merely on
account of their entire borders. The form of the leaves, however, espe-
cially as figured (PI. 11), with the lobes slightly enlarged above the
sinuses, and then gradually narrowed to a slightly obtuse point, and
the nervation also, have the same character as those of the living Liqui-
dambar styraciflua. It is true that the four species of this genus known
in the present flora have serrate borders of leaves. But three fossil
species represented by leaves with entilbe borders have been described
as Liquidambar from the TM*tiary of Europe ; and, thougli this reference
is more or less hypothetical and controversed, it shows, however, that
botanists of high standing — Unger, Watelet, . Massalongo — have con-
• sidered as probable, at least, the relation of leaves with entire borders
to this genus. It is easily seen that the leaves of Aralia Towneriy de-
scribed in this paper (PI. IV, fig. 1), have a relation of shape or general
outline to those of Liquidambar integrifolium ; and this apparent simi-
larity can but suggest the possible reference of all these and like forms
to the geuuB Aralia. I may admit this reference as probable for the two
leaves figured in Gret. FL, PI. XXIX, figs. 8 and 9, which are compara-
ble, by their primary nervation, to those of Aralia cancreta^ sp. no v.,
PI. IV, figs. 2 and 3. But though we have now a large number of speci-
mens referable to divers araliaceous types, there is none as yet with
leaves divided into lanceolate acute lobos like those which are figured
in PI. II, Gret. Fl. The reference of these leaves to Sterculia has been
proposed also, from analogy of forms to some species of this genus.
The presence of one well characterized species of Steroulia in the Greta-
ceous flora of New Jersey, where it is in connection with numerous
leaves of Moffnolia alternansj seems to give a kind of support to this
proposition. But in this case, also, I find too evident a difference in the
characters of nervation of the palmately-nerved leaves of Steroulia with
those referred to Liquidambar, Even taking as evidence of possible affin-
ities the distribution in the same formation of leaves referable to allied
genera, we could just as well admit the presence of Liquidambar species
in the Dakota group, by the reason that other forms of HamamelideWj
324 GEOLOGICAL SURVEY OF THE TERRITORIES.
a family to which this genus belougs, are recognized in the same group.
From these considerations, I persist in regarding as ancient, primitive, or
derived representatives of a species of Liquidambar the fossil leaves de-
scribed under this generic name, until other specimens, if any are found,
may point, by a variation of characters, to another more evident rela-
tion.*
A number of vegetable remains of the Cretaceous are evidently
referable, by their characters, to Populua. The only dicotyledouoas
leaves recognized by Heer, in the specimens which he studied trom the
Lower Cretaceous formationsof Greenland, represent a Populu8. appropri-
ately specified by the name of P. primceva. From a higher stage of the
same Cretaceous formation of that country, the celebrated Swiss pale-
ontologist has described three other species of Fopulus, In bis Phyl-
lites Cr^tac^es du Nebraska, and from specimens of the Dakota group,
he ha^ recognized Populus lUigiosa^ Populusf deheyana^ and another
species still, P. cyclophylla^ described in the Proceedings of the Academy
of Natural Sciences of Philadelphia. Professor Newberry, in his paper
on the later extinct floras of North America, has described, also, besides
the doubtful PJ debeyana, three new species: PopiUusf cardi/oUoy P.
ellipticaj and P. micropkilla. The specification and the interrogative
punctup<tion applied to some of these names show that the authors them-
selves do not consider the generic reference as definitive, the character
of some of the. leaves being somewhat in disaccord with those generally
recognized in species of Popnlu% of our present time. Indeed, 8])ecie9
of this kind, like the present P. alba^ i'or example, have such multiplied
and diversified forms of leaves, such great variability in their nervation,
the mode of attachment of the petiole, &c., that they readily offer, by
comparison with fossil leaves of obscure relation, some points of affinity
which, being not found elsewhere, have tjo be considered by the authors.
Hence the doubtful references which may be, and are often rectified by
subsequent discoveries, as is prof ed by the great proportion of synonyms
appended to th6 enumeration of Puptdu^ species. To obviate this incon-
venient multiplication of fluctuating species of Populnsy I proposed a
new generic division, under the name of PopiUUeSj for the classification
of those Cretaceous leaves, numerous indeed, which, pai'taking of some
of the characters of Populus^ are nevertheless removed fr^^i this division
by some others, as remarked in the memoir. f Populus lancastrieruit
was considered as a legitimate species of the genus, and in the new
division were described Populiies elegans^ P. ovata^ P. quadrangHlaT%9^
P. JUjthellata^ and P. sahsburicdfolioy with P. cyclophyllaj represented by
leaves which I considered as answering to the description of this species
by Ileer.
This first memoir on some Cretaceous fossil plants from Nebraska
had to be prepared, at a short notice, from a limited number of speci-
mens. Since its publication, I have had opportunity to study the
specific forms of this Cretaceous flora by comparing a very large number
of specimens, and have thus recognized a more evident affinity of some
of those leaves referred to Populites with other generic divisions. The
only Populitea lancastriensis and P. eUgam which Schimper considers as a
true PoptUtis are preserved in this genus, while Populites cyelaphylla and
P. ovata^ appearing rather related by their characters to the Ampelid&t,
are described under a new generic division. The leaves represented by
these species have, indeed, by their craspedodrome and subpalmate ner-
* Fragments of leaves closely allied to this form are described as Phyllites in Reiufl^
Versteiu, PI. LI, figs. 4 aod 5.
t Am. Joar. Sci., vol. xlvi, Jnly, 1868, p. 93.
LKfiQUEREUx] REVIEW OF CRETACEOUS FLORA. 325
vation, and by their base narrowed to the petiole, a more evident
affinity to species of CissuSj or VitiSj than to those of Popultis.
In regard to the distribotion of FopuluSj to which is referred the most
ancient dicotyledonous leaves known as yet, that of the Lower Creta-
ceoas of Greenland, it has, as said above, three s{)ecies known already in
the Upper Cretaceous of that same country, and five or six in the
Dakota group. It has, however, not been remarked in any Cretaceous
flora of Europe. It is not mentioned in the review of the genera repre-
sented by the, as yet, undesciibed species of Aiz la Chapelle, and no
form even distantly related is described in the Lower Paleocene flora of
Gelinden. It has, however, one species in the Eocene flora of Sezane,
and increases in the number of its representatives in all the stages of
the Miocene. As far as we know it, till now, it has few species in our
Lower or first American Tertiary group, the Eocene; a large propor-
tion, eight per cent, of the species, in the second ; still more, or twelve
per cent., in the third ; and is scarcely present in the fourth, the Green
River group.
The presence of willows, species of Salix, in the flora of the
Dakota group is not controverted; the reference of leaves by which
the genus is represented in this tbrmation is evident. As it is seen
in Cretaceous Flora, p. 60, PL V, figs. 1-4, 1 have described as refer-
able to one species only, a number of leaves somewhat different in their
size and their shape. As the specimens representing them are from the
same locality, and as I recognized upon some of them fragments of leaves
with all differences of size, forms, and even consistence and color,
I considered them as mere variations of leaves of a same tree. Dr.
INewberry has from the same tbrmation four species which, he says, he
has chosen to regard as distinct, for geological convenience. No salix
has been recognized as yet in any stage of the Cretaceous of Green-
land ; but one species, ISalix Hartigiiy Denk, is from the qnader sand-
stein of Germany, and another, 8ah'^ Goetziana^ Heer, from Qnedliu-
burg. The genus is therefore sparingly represented in Europe and
North America in Cretaceous floras which are considered as nearly
synchronous. The other genera of the Amentaceae, Betula, Alnus or
Alnites, Myrica, Qnercus, Fagus and Ficus, to which leaves have been
referred in the Cretaceous Flora, do not require any observations. In
this case, as in all the determinations of fossil plants, the characters of
the species are not always satisfactorily established, but the generic
affinities have been recognized or passed without any marked criticism.
The generic relation is especially positive for the remains referable to
Myrica, which was already represented in the Cretaceous Fiora by one
fragmentary leaf and by seeds, and to which a fine new species is added
in this memoir. It seems equally so for Quercus or its pcHsuliar division,
Tkryaphyllum^ of which we have two new species, and for Ficus^ to which
one species is added.
Specimens of leaves referable to Platanus have been found in moder-
ate proportion both in Nebraska and Kansas. The first was described by
Heer, in the " Phyllites du Nebraska," as Platanus Newberryi^ from a very
incomplete fragment. The accuracy of this determination was, however,
subsequently testified by the discovery of more complete leaves figured
in Cretaceous Flora, PI. YIII, figs. 2 and 3, and PI. IX, fig. 3, which show
the narrowed base descending along the petiole lower than the i>oint
of union of lateral primary veins, and also the tendency to a three-lobed
iiivision, characters which were not observable in the fragment which
Professor Heer had for his examination. To this fine species have
been added: Platanus primcevaj described from leaves so remarkably
326 GEOLOQICAL SURVEY OF THE TERRITORIES.
similar to those of P. aceraides^ of tbe Miocene, that I was at first
dispoRed to consider them as identical ; then, P. Heerii^ rare, like the
former, and found as yet only along the blufGs of the Salina River ; P.
obtimloha^ from a unmber of somewhat fragmentary specimens from
Beatrice, ^Nebraska, all representing leaves of about the same size and
of the same characters ; P. affiniSy P. recurvata^ and P. diminutiva. All
the species are described and figured in Cretaceous Flora. The last one
as remarked in its description may be a dwarfed form of P. primtera or
P. Heerii. The leaf appears as gnawed along the veins by insects or
perhaps by a parasite fungus. Its specification is not iK>sitive and is
subject to criticisms. The base of the leaf is rounded to the petiole,
a character as yet unique for a species of this kind. P. recurvctt^
should, following the opinion of my honored friend Count Saporta, be
referred to the AraliceaB by a more intimate affinity to Araliopm
species; and Flatanus affinis seems now, alter the examination and
comparison of a number of specimens from Kansas, more evidently
referable to the Ampelidece than to the Platanece. Therefore these two
last species are now eliminated from this generic division. I persist in
considering P. Heerii and PL ohtusiloba as two difi'erent species, thoug'b it
has been suggested that the last was probably a mere variety of the
first. The identity is denied not only by the facies, and the nervation
of the leaves, but especially by the thinner texture of those of P.
ohtusiloba. The fact, that the numerous specimens representing it are
all from the same place in Nebraska, and that P. Heerii has not been
found in this State till now, confirms this separation. In regard to this
last species, Professor Geinitz has remarked in the Isis, J 875, p. 558,
that paleontologists might perhaps recognize in it a Credneria, There
is some similarity in the general outline of the leaves, indeed. But this
might be said of many of tbe generic forms of the Cretaceous, which seem
to refer to a few difterent types, or to present in one leaf the characters
which we now generally find isolated in separate vegetable groups.
The genus Credneria^ known as it is to me by what is described in tbe
vol. y, of the Paleontographica, by Stiehler, includes species with cord-
ate or subcordate leaves (none narrowed to the petiole), and bearing
above the base two or three true secondary veins in right angle to the
midrib. In P. Heerii, the leaves are cune^iteto the base, even gradually
narrowed or decnrrent to the petiole, which thus becomes slightly winged,
and the veins under the primary nerves are mere marginal veinleta. Per-
haps the relation of this species is more marked to the genus JEtting-
hatiseniaj which, I regret to say, is scarcely known to me except by
Chondrophyllum grandidentatumy us represented by Heer in the Creta-
ceous Flora of Moletin, and by Phyllites repandug, Sternb., two forms
which have no affinity to Platanus,
In regard to its geological distribution, this genus is truly remark-
able. No trace of it is recorded as yet in the Cretaceous of Euroiie, not
even in the Paleocene and Eocene of France, so rich in fossil vegetable
remains. Its first appearance in Europe is in the Upper Miocene of
Oeningen, and of Austria and Italy, where it is represented by two
very similar forms, Platanus GuiUelmcB and P. aceroides. These two
species are present in the same lormation from the northern parts of the
Arctic lands to Italy. It is followed in the Upper Tertiary or Pliocene
of this last country by PlaianuH Aeademiee Gaud, related as originator,
perhaps, to the living P. orientalis, I have remarked above that tbe
relation of leaves of the Dakota group to Platanus has been considered
as doubtful by some European paleontologists. This doubt may have
been induced by thd understanding of the total absence of Piatanvs
leaves in the Cretaceous and Lower Tertiary of Europe, if so, it is oer-
LEsgurvRELx.l REVIEW OP CRETACEOUS FLORA. 327
tuinly removed by the presence in our lignitic Eocene of some very
beautitat and well characterized species of tbis genns: Platanus
Haydenii aud P. Reynoldtni^ Newby. Tuese species, discovered first in
the Tertiary of the Upper Missouri River, near Kort Union, are predom-
inant at Golden, Colo., by the number of specimens which represent
them, and are also found at Black Butte. The third Tertiary group,
that of Carbon, has, for the more numerous representatives of its flora,
leaves of PlaianuH Aceroides and PL GuillelnuB. Ko species of this
genus has been described from the Green Biver or fourth group ; but
we have Irom the Upper Tertiary (Pliocene) of California very fine
8i>ecimens of leaves of two species of Platanus closely related by their
characters to the living PUUanvs occidentalism Therefore, and consider-
ing the geological records, we may trace tlie origin of Platanus as far
down as the North American Cretaceous, and follow its development
through nearly all the stages of the Tertiary to our present time, by a
number of closely-allied intermediate forms.
Coming now to the Laurinem^ I have to remark somewhat more defi-
nitely on the Cretaceous species referred to this family. The relation
of some of them to the genera to which they have been referred is gen-
erally acknowledged, and the presence of the Laurinece in our Cretaceous
flora receives a kind of historical authority by that of a Sassafras in
a Cretaceous formation of Greenland; of three species of Daphno-
phyllum in that of Moletin, and of Laurus cretacea^ Daphnogene
primigenia^ Daphnites Gopperti^ in that of Niedershoena. Of the
species which have been described formerly in the flora of the Dakota
group, Laurus Nthrascencis is related to Daphnophyllum ellipticum and
/>. cra4tsinervium of Heer, while Cinnamamum aud Oreodaphne cretacea
are comparable to Daphnogene primigenia of Ettiughausen. Persea
Sternbergii is also evidently of the same family, and the two leaves,
described here below under the name of Laurus protecefoliay are indeed
allied to species of Laurtis or of Persea by their nervation, especially
by the more acute angle of divergence of the lower veins, though they
show in the grooved middle nerve a character often remarked in s[)ecies
of Ficus^ especially Fieus protogea Heer, of the Greenland Cretaceous
flora. Moreover, the fruit described (Fl. Cret, p. 74) as Laurus macro-
carpa satisfactorily completes the evidence afforded b^' the leaves, of
the existence of species of Laurince in the vegetable world of the Cre-
taceous epoch. We have, however, to eliminate of this family Lauro-
phyllum retictilatumy which appears more properly referable to Fious.
its nervation, and especially its areolation, formed of square or irreg-
ularly i)olygonal meshes by the interposition of tertiary veins between
the secondary ones and parallel to them, and the rectangular subdi-
vision of its branches, are of the same character as in Ficus Oeinitzij
Ett., Ficus protogea^ Heer, and many species of tbis genus now living
in Cuba, even Florida, like Ficus suffocansy F, lentiginosa, h. perttisoy
F. dimidiata, etc. Numerous specimens recently found in Kansas repre-
sent this fossil species in characters more precise than formerly, as seen
in its more detailed description under the name of Ficus laurophyllum.
But if the relerence of some of the above-mentioned leaves to the
Laurinew is not contested, it is not the same in regard to those which,
at first appearance, were considered as more positively related to it,
and which have been described under the generic name of Sassafras.
The question of the relation of those leaves which, by their number,
seem to be the essential components of the North American Cretaceous
flora, has been already touched upon.* But since, I have obtained
* Cretaceoas Flora, p. 77.
328 GEOLOGICAL SURVEY OP THE TERRITORIES.
from divers localities a large number of specimens representing aD
the forms described as species in the same work, and I hare now
some more data to offer to the consideration of paleontologists on
the Bnbj€'ct. From historical documents the presence of Sassafras
species in the flora of the Dakota group is as legitimately presamable
as that ot species of Laurus or Persea. In his Flora Arctica, Heer
has described as Sassafras arctica a leaf which, by its form, is similar
to those described as Sassafras cretaeeum^ as remarked by the anther,
difi'ering merely by its base somewhat less narrowly tapering to the
petiole. The nervation is of the same character. Count Saporta
considers this Greenland leaf as a true representative of Sassafras, fie
has himself published in the Sezane Flora,* as S. primigenium^ two
fragmentary leaves whose base, more narrowly tapering, is similar to
that of our S, Mudgei^ as well as the lobes which, enlarged in the mid-
dle, have that ovate-lanceolate shape so distinctly marked in the present
8. officinale. There is also no appreciable difference in the nervation.
The lower secondary veins of the middle lobe ascend a little higher in
the leaves of the Sezane flora, and unite with those of the lateral lobes
somewhat nearer the borders of the sinuses. Bnt in some of the speci-
mens of Kansas the same appearance is remarked also, and thedifference
between the more or less distance which separate from the sinuses the
branch which unites the upper division of the secondary veins, is ob-
servable upon leaves of S. officinale^ this vein being sometimes mar-
ginal, sometimes curving one to three millimeters lower than the border
of the sinuses. Comparing leaves of Sassafras officinale with those rep-
resented by Count Saporta in the Flora of Sezane and the specimens of
S. Mudgei from Kansas, it is impossible for me to recognize any charac^
ter, even any specific difference by which these leaves could be sepa-
rated. It is, therefore, not surprising that Dr. !N^ewberry first, and att^r
him Heer and Schimper, did consider Cretaceous specimens of this kind
as representing species of Sassafras. In the last volume of his superb
work on Vegetable Paleontology,! Prof. W. P. Schimper, speaking of
leaves of Sassafras eretaceum^ ot wjiich I had sent him photogniphical
designs, remarks, ^- That those leaves, very variable in size, present such
a remarkable likeness to those of S. offimnalCy now living in North Amer-
ica, that one would be disposed to consider them as belonging to an
bomologous si)ecies.'' He rightly adds that the only difference seems
to be in the thicker substance of the fossil leaves. Pjven on this {K>int
I have from Texas specimens of the present 8. cretaceous^ whose
leaves appear of a consistence nearly as thick as those of the Dakota
group seem to have been.
But now, and on another side, no species of the Laurinece family living
at our time is known with dentate leaves ; and it may be remarked, from
the figures, that the two leaves described as Sassafras Greiacetim (Cret
Flor., PI. XI, figs. 1 and 2) have the binrders of the lobes somewhat
dentate, and some of the secondary veins running into the point of the
teeth or craspedodrome. This character is still more marked in & mi-
rabile, loc. cit., PI. XII, fig. 1, a form extremely common in Southern Kan-
sas, and represented in very numerous and riemarkable varieties. In
some of the leaves the secondary veins are all camptodrame, and there-
fore the borders of the lobes are entire. In others, as seen, Pi. XI, fig. *A
the outside lateral veins are craspedodrome, and thus the boaders deih
tate, while on the inside they curve along the borders, which are entire.
• P. 366, Tab. VIII, figs. 9 aod 10.
t Traitd do Paleoatologie v6gctale, vol. iii, p. 596.
J
I.TOQUKREUX.] BEVIEW OP CRETACEOUS FLORA. 329
lu the fine complete leaf, fig. 1 of the same plate, the middle lobe has the
T'eins all camptodrome on the left side, while on the right one a few of
tbein, one or two, reach to the border, which has, therefore, one or two
ahort uodistinct teeth, and the lateral lobes are clearly dentate on the out-
side only. This evidently shows snch a disposition to variations of
nervation and border divisions, that I did formerly consider as unjusti-
fiable a specific, and still more a generic division between the leaves of
PI. XI, figs. 1 and 2, and those of PI. XII, figs. 2 and 3, of the Cret.
Flora. When, therefore, we find the same dilierences between the
leaves which represent 8. mirabile, PI. XII, fig. 1, it seems that the same
coDcinsion should follow. But in this case, with the more generally
predominant character of the indentation of the leaves, which, in some
larger specimens than the one figured, are more deeply cut by divisions,
like pointed lobes, there is still another one, remarked on a specimen
recently discovered, which seems to more forcibly separate these forms
from the Laurinece, and indicates a more evident relation to the Aralia-
ceas. The specimen communicated by M. Chs. Steniberg, to whose
careful and zealous researches the flora of the Dakota group is indebted
for many important discoveries, represents a large leaf which, by its out-
lines, the nervation, and the dentate borders of its lobes, is exactly like
oor 8. miraMle of PI. XII, ^g. 1. The leaf, which is much larger, how-
ever, the lobes measuring ten centimeters in length from the point of
onion of the primary nerves, greatly differs b; the forking of the lateral
nerves, from a point two and one-half centimeters above their base, and
thus forming, of course, a subdivision of these lobes into two equal parts,
or a palmately five-lobed leaf. Among the innamerable varieties in the
shape of the leaves of the living Sassafras officinale^ we 'see a constant
and gradual mode of division passing from a round or oval and entire
shape to a bilobed and trilobed one ; but, as yet, I have been unable to
observe a single case of subdivision of the lateral lobes, or to find a
palmately five-lobed Sassafras leaf. This character is, on the contrary,
tar more generally seen in the Araliacece of our time than in the trilo-
bate form of Sassafras. But in this section of Araliacece^ the Eedera^
which may be compared to our leaves, I do not know any with trilobate
leaves. Hedera turbascens^ H, discolor ^ H. argentea^ H, aurifoliaj H, jor
tropwfoliay have leaves five to seven palmately lobed, or, when occa-
sionally trifid, their segments are narrow and acuminate, of a ty|)e
related to that of Aralia tripartita of PI. I, fig. 1, of the memoir. The ref-
erence of these leaves to Araliaoeas is, therSbre, apparently obscure or
uncertain. And still, on another side, comparing the beautiful Aralia
saportanea represented in this memoir, fig. 2 of the same plate, we
see in its nervation, as well as in the indentation of the borders, &c., a
remarkable identity of characters with those of the five-lobate leaf of
Araliopsis mirabilis. Thus we have about the same degree of evidence
in regard to the relation of these fossil leaves to Aralia or to Sassafras.
Going further into this kind of investigation, we are met by a new
difficulty in the appearance of another modification in the characters of
this peculiar type of leaves. In examining the first specimens of the
species represented, PL II, fig..l,.I could but consider them as repre-
senting either Sassafras (Araliopsis) obtttsumy or 8. miraMle^ for, the
specimens being fragmentary, had only the lobes or part of them.
As long as the auricled and peltate base was unknown, the reference
of the specimen could not be dlffeient. The nervation, the form of the
lobes, their size, all is of the same character as in 8. mirabile. But
in the peltate base of the leaves, which is figured Irom a leaf pre-
served entire, PI. II, fig. 1, and from fragment of much larger ones,
330 GEOLOGICAL SURVEY OP THE TEBRITORIES.
fi^. 2, we have another character which presents the union of leaves
of this kind either with the Lautinece or with the Araliacea^ and thus it
is necessary to admit a third generic division for the classification of Ibe
vegetable remains of this new and remarkable type, which adds to itB
affinity to Sassafras and Aralia a character which relates it to Platanos
and Oredneria, by the basilar appendage of the leaves and its nerva-
tion. We have thus already in those leaves Sassafras, represented by
iS. Mudgei^ and less positively hyS. acutilohum, 8. cretaceumy and 8,
cretaceum var. obtusunij which, as seen by the description, baa to be
considered as a specific form. To Araliopsis are referable S. mirabik^
with the dentate 8, cretaceum and Platanus rectirvata; and to the
new generic division, under the name of Aspidiophyllumj those leaves
which, either Arulia or Sassafras by their upper trilobate part^ are
forcibly separated from these genera by their auricled peltate ap|)eud-
age. Still, the subdivisions in the classification of these peculiar and
so-called Sassafras leaves, have to be pursued farther, for by degree and
by the gradual obliteration of their lobes, they become round or truncate,
or broadly pointed at the top, preserving more or less the narrowed base,
tapering to a long petiole, and the trifid craspedodrome nervation from
a distance above the borders, and thus they become more evidently
related to other vegetable orders. One species is a true Hedem,
another goes to the HamamelidecBj and a number have their affinity
witb the Ampelidece,
The characters of the leaves of this order, especially those of Cisr
sns, are somewhat obscurely represented in Sassafras HarJcerianum^
Cret. Flor., PI. XT, figs. 3 and 4; PI. XXVII, fig. 2, and in &
obtuHum, PI. XIII, figs. 1^ to 4; more distinctly in Cissites acuminatus^
PI. VIII, fig. 1 ; and C. Heeriiy PI. VI, fig. 3, two new species de-
scribed in this memoir. They appear to constitute an indivisible
group with the two former ones. Some of the leaves formerly de-
scribed as PopuUtes are also referable to this section, or to another
less exactly defined ; Ampelophyllum^ allied by some of its characters
to Hedera^ by others to Credneria; thus intermediate to the Ampetidm
or the Tiliacew; by the areolation to OreviopsiSj and also more distantly
to Chondrophyllum of Beer, as remarked in the description. From tbis
it is perceivable that this Sassafnis type, which at the beginning
was regarded as simple, well defined, and limited in its character, is, oo
the contrary, multiple and representing forms which, as far as the re-
searches increase the discoveries, indicate affinity to a number of differ-
ent genera or orders of the vegetable reign. Considering for example
Sassafras acutifolium of Cret. Flor., PI. XIV, which, from specitneus
representing intermediate forms between fig. 3 and fig. 4,1 was disposed
to consider as a mere variety of 8. Mndgei^ and passing to fig. 7 of PI*
XXX, evidently of the same generic type, and then to fig. 1 of PL VlII
of this memoir, where is the difference or the point of separation to be
marked f Tbe type of AmpeUdce is quite as distinct as that of tbe
AraliacecB in this peculiar group ; but both are recognized it seems
merely in the extreme and opposed limits of their modifications.
The same remark is applicable ju^t as well to the leaves which have
been described in the Cret. Flora under the generic name of Frotophtflr
lum. The disagreement in the affinities of its species has been exposed
in the remarks following the description of the genus. I have now to
add still to this division two leaves recently communicated from £ao-
sas, represented, PI. Ill, fig. 1, and PI. VIII, fig. 4. They fully confirm
the former observations. By the outline of the leaves, their craspedo-
drome nervation, and the presence of two pairs of secondary veins
1JWQUBMUX.J KEVIEW OP CRETACEOUS FLORA. 331
under tbe primary ones aad ia right angle to the midrib, they represent a
81>ecie8 of Protophyllum; but the border base of the leaves is trancate,
not sabpeltate, and by this difference the leaves are rather referable to
Gredneriay from which, however, they differ by the veins all craspedo-
drome as well as their divisions, and by the truncate, not cordate, base
of the leaves. I have formerly published a short description of these
leaves nnder the name of Credneria t mierophylla. It now seems that
by their evident relation to Frotophyllum quadratum^ they have to be
admitted in the generic division, an opinion which may be put at naught
by the discovery of specimens pointing to another reference for these
leaves.
We have, also, an addition of three new species to the group of Cre-
taceous plants described under the genericuame of Menispermites. In this
case, however, there is no difficulty whatever in conformably uniting into
a definite group the characters of the leaves which, round, ovate, or oval,
with borders entire or undulate, have a common generic affinity, indi-
cated by their nervation. In order to more clearly bring into view
tbe relation of the undulate-lobed forms of leaves descril^d in Gret.
Flora, PI. XX, figs. 1-4, and PI. XXV, flg. 1, I have represented, PI.
YII, fig. 3, of this paper, a finely and wholly preserved leaf of Mentsper-
mites (^tusiloba^ which, though small, is easily identified with the large
one of PI. XXY, fig. 1. Now, comparing it to figs. 3 and 4 of the
present PI. V, the identity of nervation is defined by the five basilar
veins, with a thin pair of marginal veinlets underneath ; and by the up-
ward direction of the internal lateral veins, which, in fig. 3 of PI. YII,
ascend to above the middle, pass still higher in the short oval leaf,
PL Y, fig. 3, and reach nearly to the obtuse point in fig. 4. The subdi-
vision of the tertiary veins is in all the leaves of the same type, and the
shape of the leaves or their outlines are mere modifications, depending
upon the direction of the veins. The leaf, PI. YI^ fig. 4, is peltate
from the point of attachment of the petiole near the middle. The char-
acter of the nervation remains, however, the same. It is somewhat ob-
scured in the figure, from indistinctness of the specimen. But a larger,
finer leaf of the same species, has been more recently procured by Mr.
H. G. Towner, of Clay Center, Kansas, another of those proficient ex-
plorers whose researches have greatly increased the materials for the
elucidation of the Cretaceous fiora. This leaf, preserved in its whole
is nearly round, with slightly undulate borders, and the nervation
is marked by three pairs of primary veins, on each side of the mid
rib, and nnder them by one pair of true marginal veinlets curving on
each side toward the borders. Comparing, therefore, this peltate leaf
with that of PI. Y, fig. 3, the position of the petiole is the only notable
difference. The peltate form of these round leaves might perhaps sug-
gest the fitness of some slight modification in the characters assign^
to the genus Pterospermites^ in tbe Cret. Flora, p. 94, the leaves l^ing
here rounded or subcordate at base. The difference is immaterial, and
is remarked even upon leaves of the same species of MewMpermum of our
epoch. These round peltate leaves, for example, are so much like those
of living species of Ciasampelosj that they rather prove the adaptation
of this generic division to all the Cretaceous leaves which I have referred
to it.
The Magnoliacece, aa order of the same class, are equally numerously
and definitely represented in the North American Cretaceous flora in
about the same proportion as they are in that of Europe. Magnolia al-
temans and if. Gapellini have been described by Heer in his Phillites
du Nebraska 3 and since, these two species have been recognized over
332 GEOLOGICAL SURVEY OP THE TERRITORIES.
the whole explored area of the Dakota group, as also in the lower stage
of the Cretaceous of New Jersey, and in the Upper Cretaceous of Green-
land. Two other species have been described from the Dakote group:
one, M. obovata, by Dr. Newberry, in his Ancient Floras ; another, If.
tenulfolia^ in Cret. l^lora. in Europe the leaves referable to this
genus are of adififerent type than ours, larger and more beautiful. Two
species — M. ampl\folia and M. speciosa — are described by Heer in the
Flora of Moletiu, there represented by leaves and fruits. Coaut Sa-
porta considers also as a Magnolia Phyllites plagiavs^ Ung., of the flora of
Gosau.
To the same order belong Liriodendronj so easily recognized in the
peculiar form of its leaves. Its Cretaceous origin, or rather existence, is
marked in the Dakota group by a number of specific representatives
locally and distantly distributed. At least, though the first lot of Cre-
taceous specimens sent from Nebraska and Kansas for examination had
many fragments of the species described in Cretaceous Flora, I have
since received only a small leaf found in Kansas by Dr. Mudge, refera-
ble to L. MeeJcii. This genus is not as yet represented in the Cretaceous
floras of Europe, nor in that of Greenland.
To the class of the Columniferew, taking altogether the three orders,
SterculuBj ButtnertacecBj and Pterotipermm^ are apparently refei-able the
forms described under the generic name of Protophyllum^ as well as the
true Oredneria. The Sterculiacece are more distinctly represented by a
leaf described in this memoir as Sterculia cretacea. Though the nerva-
tion is obsolete, the mode of division of the leaf in equal linear diverg-
ing lobes is like that of species of this genus, which has also a well-de-
fined species in both stages of the Cretaceous of New Jersey. To the
Tiliacece^ the leaves described as Greviapsis Haydenii have an evident
affinity of characters.
The relation of Cretaceous species to the following and last classes of
the vegetable reign is not very clearly defined. To the Acerea: is refera-
ble Negundoide% aeutif alius of the Cretaceous Flora. The leaf, however, as
seen from the figure and description, is too fragmentary for a satisfactoiy
determination of its characters. Acer antiquum is described by Etting-
hausen in his Cretaceous Flora of Kiedershoena. But even from the
opinion of the author the reference is uncertain. The leaf rather resem-
bles a deformed form of Quercus or of Idriodendron. Heer has from
the Upper Cretaceous of Greenland a Sapindus prodromus, represented
by one leaf only, which, however, has evidently the character of the
genus. To the Rhamnin the leaf described as Rhamnus tenax^ in
Cretaceous Flora, is probably related, and this relation seems con-
firmed by the presence of Celastrophyllum and Hex species in the
same formation. Count Saporta, however, considers this leaf as show-
ing more affinity of form and nervation to Salix. To the Anacardia^
we have probably to refer as Rhus debeyafia, that species described as
Populus and as Juglans^ as seen in Cretaceous Flora, p. 110. I have not
obtained from the Dakota group any new materials comparable to this
form, especially common in Nebraska. But I have seen a veiy fine
specimen got out of a deep tunnel in Oregon, presenting upon its sur-
iace, with the details of nervation and areolation, some punctifbrm small
protuberances, apparently oily glands, like those remarked upon leaves
of the living Rhu^ aromatica and other species of this genns. A
species of Rhus is described from the Cretaceous of Greenland by
Heer, while considering historical authority, we have the same evidence
in favor of Juglans^ by a species of this genus in the Cretaceous floni of
Moletin. Of the RosiflorecBy we have from the Dakota group one lent and
I.KSQ17EBKUX.] ENUMERATION OP CRETACEOUS PLANTS. 333
one frait described as Prunus, I have recently' received from M. Towner
a Iruit of the same character upoo a specimen bearing leaves of Aralia
Totoneru The MyrtiflorcBy as well as the Legumino^ce present by a num-
l>er of species in the Greenland Cretaceous, have not been till now posi-
tively recognized from Kansas and Nebraska specimens. The few
groups not considered in this review have been remarked upon already
in the Cretaceous Flora, and the former views, in regard to the leaves
referred to them, have not been modified either by the remarks of Eu-
Topeau authors or by the discovery of new materials.
§ 2. Description and enusieration of Generic and Specific
Divisions.
With the descriptions of the new forms illustrated by the plates,
this part of the memoir contains an enumeration of all the species
established till now from the vegetable remains of the Dakota group,
viith remarks suggested b^ the examination of the materials discovered
aiuce the publication of the Cret. Flora*. In order to give to this
euumeration the value of a synopsis of this flora, I have added to the
Bpeeific names short descriptions, either copied in full or somewhat
moditied from those of the same volume.
For the discovery and the communication of the new materials, all
collected in Kansas, the thanks of paleontologists are due especially to
Messrs. Ch. Sternberg, of Fort Barker, H. C. Towner, of Clay Center,
and also to Prof. B. F. Mudge, of Manhattan.
CRYPTOGAMOUS.
THALLOPHYTES.
ZONABITES DiGiTATUS, Brgt., Cret. Flor., p. 44, PI. I, fig. 1.
Frond Jlat, memhranaeefyus^ dichoUmumSy branching in an acute angle of
divergence; divisions as broad or broader than the mainaxis^ linear^ entire^
obtuse^ slightly enlarging upward.
The reference of this species to that described by Brongiart from the
Oolithe is contested especially by reason ol difference in the geological
station.
PILICES.
Lyoodium tbichomanoides, Lesqx., Cret. Flor., p. 45, PI. I, fig. 2.
Pinna linear^ from the truncate base to the middle^ enlarged and lobed
Hpward by the forking of tlie middle nerve; veins broadly oblique^ distinct^
simple or forking from the base.
Hymenophyllum cretaceum, Lesqx., Cret. Flor., p. 45, PI. I, figs. 3, 4.
Frond subcoriaceous^ pinnae linear oblongj pinnately divided into oblan-
ceolate or cuneiform oblique pinnules, decurring to the convex, slightly
winged radiis^ more or less deeply bi-trilobate; lobes obtuse, simple-nerved.
This, like the former species and Sphenopteris corrugata, Newby., are
contestable on account of the deficiency of the specimens.
Pecoptebis Nebbaskana, Heer. Cret. Flor., p. 46, PI. XXIX, fig 5.
Pinnce coriaceous, linear-lanceolate obtuse, alternately equally lobed;
lobes more or less disjointed, turned outside, obtuse; middle vein thin, un-
dulating; divisions alternate, ascending to the borders.
* Seport of the United States Geological Sanrey of the Territories, by Dr. F. Y. Hay-
den, vol. Yi, CretaceoQS Flora (1874).
334 GEOLOGICAL SURVEY OF TOE TERRITORIES.
Gleighenia Kurriana, Heer., Cret. Flor., p. 47, PI. I, Figs 5-5^
Frond pinnate ; pinnce long^ liiiear^ pinnately equally lobed ; lobes nearljf
at right an^le to t^ie rachis separated to near the base ; '}nedial nerve ^Aicfc,
pinnately brafichiugj veins forking at the middle.
Gleichenia Nordenskioldi, Heer, Flor. Foss. A ret., p. 50, Tab. IX,
figs. 6-12.— PI. II, fig. 5.
Frond slender dichotomous^ bi-polypinnate ; ultimate pinnw aUematet
rigidj open, linear ^ parallel; leaflets free^ oblong obtuse^ rounded at their
base^ inclined upward^ coriaceous; secondary veins few ^ three or four pairs,
il^e lower forking^ tJie upper simple.
This species is very distinct from the former, and the differences in
ttie characters easily seen even in onr fragmentary specimens. In the
one figured here, the pinnules are separattnl to their base, and not mere
lobes as in the former ; they are turned upward, and by the upper baailar
border they compress the rachis, which becomes evidently fleznous, in
onr specimen, at least ; the veins, also, are more distant, or less divided.
Th$> fructifications of this fine fern are marked upon the specimens of
Greenland by two large round sori on each side of the middle nerve,
near the base of the leaflets. There is no difference whatever in any
of the characters of the Kansas specimen with those of the Greenland
form. Even the undulation of the primary rachis distinctly remarked
in Tab. IX, fig. 7, of Heer's flora, is equally distinct in the primary
rachis of the fragment figured here. This species has been observed on
specimens from the Lower Cretaceous of Greenland only, wherefrom
Professor Heer has described thirteen species of Gleiclienia^ while only
two were found in the specimens of the Upper Cretaceous of the same
country.
Habitat, — Near Fort Barker, Kansas, Chs. Sternberg.
PH^NOGAMODS.
CYCADE^.
Pterophyllum (!) Haydbnii, Lesqx., Cret. Flor., p. 49, PL I, fig. 6.6«.
Frond linear ^ simply pinnate ; raehis rugose^ half an inch broad or more,
marked by circular dots in vertical rows^ and regularly placed about half a
centimeter distant, apparently scars of the points of attachment of the
pinnce; pinnce (or leaves) entire, oblong, oval obtuse, slightly arched o%
the lower side, flat, attenuated at the round point of connection to the
rachis, regularly and narrowly striated lengthwise.
Of this peculiar organism, no other part has been discovered excef)t
the fragment figured. Professor Heer regards it as unreferable to tbe
Gycadece, on account of extraordinary broad stem, and supposes that it
should rather be considered as a Conifer, of the section of tbe
Araucarites. This opinion seems confirmed by the presence xx\Hm the
same specimens of the cone described here below as Abietites Ernestine,
both cone and branch being originally described as representing a
same species related to Pterophyllum Ernestines of Stiehler, described
from similar fragments in the Paleontographica.
conifers.
Abietites Ernestinjb, Lesqx., Cret. Flor., PI. I, fig. 7.
Cone oblong, abruptly narrotced to a short pedicely scales broad, truneate,
appressed and imbricated. *
UESQUERKUx-l ENUMERATION OF CRETACEOUS PLANTS. 335
Sequoia Formosa, Lesqx., Cret Flor., p. 50, PI. I, figs. 9 and 9*.
Cone spindle-shaped^ tapering upward from above the base and more
rapidly narrowed to a short petiole / scaies closely oppressed and imbri-
cated^ rhomboidalj margined.
Sequoia Reichenbachi !, Heer, Cret. Plor., p. 61, PI. I, figs. 10, 10^
Conesniall^ oblong, oval; receptacles ovalj pointed at both ends; foliaceous
scales crumpled, deeply embedded into the stone; seeds small, oval-oblong.
In comparing this cone to the figures given of the species by Professor
Heer in bis Moletin fiiora, the reference was made especially to fig. 3 of
PL I. Professor Heer remarks rightly that there is no relation between
these cones of Moletin and the one of Nebraska, the former being much
larger and the scales therefoie longer, and that thoagh representing ap-
parently a species of Seqnoia, the specific name sboald be left undeter-
mined until better specimens have been discovered.
Sequoia fastigiata ! Sternb., Heer, Mol. Flor. p. 11, PI. I, figs. 10,
13.— PL 111, figs. 2 and 8.
Branches erect, slender ; branchlets filiform, fastigiate, crowded ; leaves
loosely imbricated, short, decurrent at the base, broadly lanceolate, acumi-
nate, subfalcate, or more or less curveS upward ; nerved.
We know of this species only what is seen in the small branch figured
8 and 8®, for the cones of the same plate, fig. 2, though observed upon
specimens of the same locality, have not been found in connection with
the branches bearing leaves. The leaves appear of the same form and
characters as those represented by Heer in his Moletin Flora, loc. cit, and
as those from the Greenland Upper Cretaceous flora by the same
author, p. 102, PL XXVII, figs. 5 and 6, merely dififering by the presence
of a middle nerve recognizable upon the specimens of Kansas, and which
is not seen upon the leaves of Greenland and Europe. This mode of
division of the branches is the.same, and in comparing the cones of our
^g, 2 with those figured by Heer from both Greenland and Moletin
specimens, the likeness appears very great indeed. As the leaves of
this species are very variable in size and the middle nerve generally
perceivable with great difficulty, I am not disposed to separate it from
the only difference of the more distinct middle nerve of the leaves, and
I consider it as very probably the same as that of Moletin. Heer re-
marks a character also recognizable upon the fragment from Kansas,
viz, the difference of the size of the leaves upon different parts of the
branches.
Habitat. — Kansas, Clay Center, jET. C Towner.
Sequoia condita, sp. nov., PL IV, figs. 5-7.
Brandies rigid, pinnately divided ; branchlets slender, filiform, open or
oblique; leaves either short, oblong pointed narrowed to tJiedecuf ring base,
appressed to the stem, or longer, subulate acuminate, open and slightly fal-
cate, nerveless ; cone small, oval-oblong, scales rhomboidal, acutely mam-
millate.
After briefly describing this species for the Bulletin Xo. 5, second
series of the Geological Survey of the Territories, I received from Clay
Center a number of fragmentary specimens satisfactorily showing its
various characters. They prove that the fragment, PL IV, fig. 7,
which I had considered as representing a different species, and described
83 doubtfully referable to Sequoia subulata, Heer, of the Greenland
Cretaceous flora, belongs to the same species as the fragment, fig. 5«
336 GEOLOGICAL SURVEY OF THE TERRITORIES.
lu this one, the leaves closely appressed to the stem, either imbricated
or distant, two millimeters long, one millimeter broad in the broadest
part above the middle, have an oblong, elongated rhomboida! form, with
a short, acute point, and gradually taper from above the middle to the
decnrrent base. In other specimens they are, as in fig. 7, linear, aco-
minate, or subulate, four to five millimeters long, less than one millimeter
broad, decurring at the base, more generally halt' open and straight,
sometimes, however, slightly falcate. Passing downward uiK>n the
same branches, these leaves become shorter, more closely appressed to
the stem, the point only being turned outside, and they then are similar
to those of the enlarged fig. 5, differing merely by the size. A num-
ber of fragments of cones, also, one ot them preserved nearly whole,
and still attached to a branch, prove that fig. 6 represents rather au
unopened young fruiting catkin of the same species than a male one,
as I supposed at first. The ripe cone is fourteen millimeters long, five
millimeters broad, cylindrical-oval, with scales deeply impressed into
the stone, and the apophyses three to four millimeters broad and nearly
as long, rhomboidal in outline, acutely narrowed on both sides, bearing
in the middle or a little above a pointe<l ^t) mammilla, marked by a small
hole in the stone. Another cone, cut in its length exposes the thick,
smooth (not crumpled) foliaceous«appendages, and the receptacles of
the seeds, which are large and similar to those of the cone described in
Cret. Flora, Tab. I, Fig. 10 and 10^, as Sequoia reichenbachu Indeed,
the form of the opened cone is the same ; this last one appears only some-
what longer. All the fragments representing this species are, like the
cones, deeply impressed or molded into the stone, even the leaves,
which often penetrate it by their points. They appear thus of a thick
coriaceous consistence. Their outside surface is, of course, the only
part whose impression is represented. It is half-round or slightly chan-
neled; the inside surface, if exposed, could perhaps show a middle nerve.
This species is distantly related to Sequoiafastigiaia^ Sternb., described
above, dififering by the pinnate mode of division of the branches, the
form of the leaves, etc. The fragment, tig. 7, has a likeness to the one
represented by Heer in his Flor. Foss. Arct. Ill, PI. XXVII, fig. 9«, as
Sequoia rigida, a species, however, far different by the visible nerve of
its leaves and by the large size of its cones.
Habitat. — Fort Barker and Clay Center, Chs. Sternberg, E. C.
Towner,
PiNUS QUENSTEDTI, Heer, Moletin Flora, p. 13, PI. II, figs, 5-9, and
Tab. HI.— PI. Ill, figs. 6, 7.
Leaves by^ five^ very long and slender y linear^ deeply nerved^ the base in-
closed in a long cylindrical sheath; cones cylindrical, very long, scales tcitk a
broadly rhomboidal shield {apophyse) acute on ilie sides^ mammillate in the
center.
The specimens representing this species are numerous, bat all
more or less fragmentary. The attachment of the base of the leaves by
five is more or less distinctly marked by the long sheaths forming deep
holes into the stone, the orifice of which has remains of leaves ; these
are very numerous, always seen by their deep impressions, half cylin-
drical on the back, channeled and deeply nerved on the inside, as
marked in the enlarged figure 7^ The length of these leaves is not rec-
ognizable from our specimens, which have mere fragments, five to eight
centimeters long; but Prof. Heer, who had complete splendid speci-
mens for his description, gives the measure at twenty centimeters;
their width being scarcely one millimeter. The cylindrical cone is
lb:qukiikux.] ENUMERATION OF CRETACEOUS PLANTS. 337
twetity-two millimeters broad, gradually tapering to the base, and from
what is seen from large stones perforated by its impressions, its length
was at least fifteen centimeters. Most of the specimens whereupon it
is represented show it curved or paltate. It is the only difference
remarked in comparing it to the cones, represented by Heer, from the
Moletin flora, and which are straight. In the flora of Gelindon, by
Saporta and Marion, the authors remark, p. 19, that this species does
not differ in any character from the living Mexican species, with qni-
uute leaves, which now compose the section of the Pseudo-strohus.
Habitat. — Mostly and more generally found near Fort Barker, by
Chs. Sternberg; some leaves are mixed with the specimen of the former
species sent by H. C, Towner from near Clay Center.
Glyptostrobus graoillimus, Lesqx., Cret. Flor. p. 52, PI. I, figs. 8,
lJ-11'.
Branches fastigiatej very slender ^ threadlike^ much divided; leaves
imbricate^ appressed, embracing the base^ linear-lanceolate^ more or less
abruptly pointed; cone narrow, cylindrical.
No new specimens of this remarkably fine species of Conifers has been
found ; its reference is therefore still uncertain. I consider it, from the
affinity of its characters to tho^ of Frenelites reichii of Ettinghausen, as
identical with this species. But its true relation, even if identity wa€
positive, is not the better ascertained for that. Schimper admits* this
Frenelites as a synonym of Sequoia fastigiata, Stemb. The presence of
both these species in the Cretaceous of Kansas would perhaps give to
this opinion a kind of authority. But it seems contradicted by the great
diflerence in the appreciable characters of these remains as far as they
are known. We can, however, say nothing in regard to the afiinity oi
this Olyptostrobus or Frenelites, as long as its cones are unknown. If
the scales found in connection with the branchlets and figured in Cret.
Flor. PI. I, fig. 8 (enlarged), belong to it, they rather resemble those of
the cones of Sequoia condita, which, however, are longer, narrower, and
of a different type than those of S. fastigiatu.
Inolepis ! species. PI. IV, fig. 8.
CoTie or fruit globular, five-costate, attaclied to a branch mixed with un*
determinable remains of conifers.
The specimen is distinctly represented in the figure ; it shows the
deep semi-globular impression of an apparently unopened fruit, marked
in the length by five obtuse costo) or narrow ribs coming together, and
disapi)eariug below the top. The other fragments attached to the stem
above this impression appear like the scales of an opened cone or fruit
of the same species. I find nothing to which this can be compared but
the cross-section of a cone of Inolepis imbricata, Hej»r., Flor. Fosa. Arct.,
PI. YXl, fig. 16, supposing that the impression of our specimen repre-
sents the outside surface of a cone of this kind deprived of its scales. This
affinity is indeed a distant one, and the comparison is acceptable merely
on account of the connection of this vegetable organism with a mass of
decayed and broken remains of Conifers.
Phyllooladus subintegripolius, Lesqx., Cret. Flor., p. 54, PI. I, fig.
12.— Tab. II, tig. 4.
Leaf coriaceous, oval-oblong, tapering from below the middle to a sliort
thick petiole ; undulate toward tlie top and abruptly rounded; middle nerve
* Puleontolugie Vegetable, vol. ii. p. 316.
99 TT
338 GEOLOGICAL SUKy£Y OF THE TERBITORIES.
narrow mid scarcely distinct except near the hose where it bccomett inftatei;
lateral veins close and thin^ a few of them more prominent and thicker^ aU
rvnnin{i to the borders in an acute angle of divergence and nearly straight.
The fragment figured here is the second specimen of a leaf of this
kind observed in the Cretaceous. Its relation seems authorized.
MONOCOTYLEDON US.
Glumace^.
Phragmites CRETACEOUS, Lesqx., Cret. FI., p. 55, PI. I, figs. 13 and
14 ; PL XXIX, tig. 7.
Leaves and culms of various size, tlie leaves gradually narrowed to an
obtuse pointy doubly veined ; primary veins thickish or inflated by tA« epi-
dermis, under which only the intermediate secondary veins, three or/our^
may be discernable.
The reference of the fragment of stem and the knot, PI. I, figs. 13 and
14, and of the leaf; PI. XXIX, fig. 7, of the Cret. Flor., has been contested
as very uncertain. The exactness of the determination, however, is
rendered probable, at least, by the presence of fragments of the same
kind in the Upper Cretaceous of Greenland, and described by Heer, Io(.
city p. 104, PI. XXVIII, figs. 8, 11, as Arundo grosnlandica^ The leaf, fig.
11, and its point, fig. IP, have the same form as that of our fig. 7. I have
more recently still received a number of fragments of small culms, one to
one and a half centimeters, representing still more clearly the chars&cters
of the species. The distance between the primary veins is variable.
DlOSCOREiB.
DioscoREAf CRETACEA, Lesqx., Cret. Flor., p. 50, PL XXVIII, fig. lOl
Leaf coriaceous, entire, nearly lound, slightly emarginate ai the poiM,
broader than long, rounded or truncate at the base; veins apparently aU
from near the base, the outside ones curving parallel to the borders atid
sparingly branching ; tlie other parallel to each others, simple^ curving in
the same way in ascending, connected in the upper part by arched nervilks,
the inner ones aerodrome.
PALMiE.
Flabellaeia! minima, Lesqx., Cret. Flor., p. 50, PL XXX, fig. 12.
Rays narrow, splitting in laciniw; veins promineiit, parallel; intermediaii
space concave, marked by uidistinct veinlets parallel to tlie primary reins.
The reference of these small fragments to the Palm family is gen-
erally contested.
DICOTYLEDONOUS. APETALEiE.
ITEOIDE^.
Liquid AMBAR integrifolium, Lesqx., Cret. Flor., p. 50, PL II, flg*
1-3; PL XXIV, fig. 2.
Leaves coriaceous, variable in size, deeply five palmately lobed; ditisiosi
orate lanceolate, obtusely pointed, entire, separated by obtuse sinuses ; in/^
rior lateral lobes in right angle to the midrib ; nervation eamptodrome.
\
LESQUEBEux] ENUMERATION OP CRETACEOUS PLANTS. 339
PopuLiTES LANCASTRraNSTS, LesqK., Cret. Plor., p. 68, PI. Ill, fig. 1.
Iieaf large, coria4:eouSj broadly cordate, apparently pointed, entire or with
slightly undulate borders; nervation pinnate^ subcamptodrome.
According to Schioiper, this species is a true Populus.
PopuiiiTBS ELEGANS, Lesqx., Oret. Flor., p. 60, PI. Ill, fig. 3.
Iteavea broadly oval or nearly round, narrowed by an abrupt curve to a
long, slender petiole ; borders entire, undulate ; nervation pinnate, subcamp-
todrome, the lower primary veins joining the middle nerve a little aAove the
border-base of the leaf.
Saxix protkepolia, Lesqx., Oret. Flor. p. 60, PL V, figs. 1-4.
liCaves lanceolate, gradually tapering to an obtuse point, largest at or
more generally below the middlCj narrowed to a short petiole ; coriaceous,
surface polished,
AMENTACE^.
Betuia beatriciana, Lesqx., Cret. Flor., p. 61, PI. V, fig. 5 j PL XXX,
fig. 4.
Itcaves small, rhomboidal-obovatein outline, cuneiform from the middle to
the petiole, rapidly tapering from above the middle to a point, simply dentate
in the upper part, entire to the base ; nervation pinnate, craspedodrome.
Id bis critical notes, Oonnt Saporta says that these leaves might he,
perhaps, detached leaflets of some species of Cissus or Araliopsis, the
presence of Betala leaves being improbable in the Cretaceous.
Myriga obtusa, Lesqx., Cret. Flora, p. G3, PL XXIX, fig. 10.
Leaf thick, coriaceous j shining, linear, obtuse, entire; medial nerve thick;
secondary veins thin, nearly at a right angle to the middle nerve, curving
near and along the border in marginal festoons, anastomosing, from the mid-
dle or above, with the branches of intermediate short veinlets.
Myrica cretacea, sp. nov. PL III, fig. 4.
Leaf linear lanceolate long f point broken J, gradually narrowed to a thick
petiole; minutely denticulate on the borders, secondary veins parallel, dis-
tant, at an acute angle of divergence from the flat broad middle nerve, camp-
todrome; tertiary veiiis short, anastomosing with branches of the second-
ary ones.
The figare shows the only fragment known of this species. The snb*
stance ot the leaves is sabcoriaceous, rather thick, the surface smooth
or polished; the borders, slightly reflexed, minutely denticulate,
evidently so, but not quite as deeply as marked upon the figure;
from the broad middle nerve, the secondary veins, irregular in distance
and branching, ascend, in an acute angle of divergence, about 30<^ to near
the borders, which they closely follow by ramifications. Tbe areolation
IB not distinguishable.
The leaf is comparable to Myrica (Dryandroides) Zenkeri, Ett., Ereide
Flora vonNeidersboena, p. 23, PL III, figs. 1, 3, 11, which is also publish-
ed by Heer from Greenland, in the Arct. Flora. Though our leaf 18
larger and the denticulation of the borders of a diiferent character,
in right angle to the borders not as pointed and turned upward as in
the European species, these differences might be merely local and the
species identical. A close comparison is not possible, from the absence
of the characters of the secondary nervation, on the specimens of
Europe and of Oreenlandi Ettinghausen, however, remarks that the
teeth of tbe borders are minute and acute, or slightly obtuse and close^ as
340 GEOLOGICAL SUfiVEY OF THE TEBRIT0BIE8.
in our leaf, but adds that the secondary veins are very slender (lenu-
issimi)^ while in ours they are thick and distinct.
Habitat. — Near Fort Barker, Kansas, Chs. Sternberg.
M YRio^ SEMINA, Cret. Flora, p. 63, PI. XXVII, figs. 4 & 4*.
Seeds obovaie^ a Utile more tluin two millimeters in the upper party painted
at the other sidej bordered by a narrow margin.
CUPULIVIEEJE.
Dryophyllum (quercus) latifolium, spec. nov. PL VI, fig. 1.
Leaf large^ oval, obtuse at the top and base, sinuate or obtusdy deuiaie ;
lateral veins on an acute angle of divergence, straight to the borders, branrk-
ing once or twice.
This fine leaf is coriaceous, twelve centimeters long, nine centimeters
wide below the middle, its broadest part, obtuse at the point and base,
deeply undulate, or, rather, obtusely dentate at least in its upper part
The nervation is thick, the secondary veins pass up at an angle of diver-
gence of 50^ to the borders, and enter the teeth, while the upper division
or veinlets pass under the (Minuses and follow the borders, a marked
character of the species of this section ; the nervilles are distinct thon^
thin, in right angle to the secondary veins, distant and disconnected ; tbe
ultimate areolation is obsolete. The leaf resembles somewhat by its
Ibrm Querctis Olafseni, Heer, of the Flora Arctica.
Habitat.— Fort Barker, Kansas, Chs. Sternberg.
Dryophyllxjm (quercus) PRiaroRDiALE, Lesqx., Cret. Flora, p. 64,
PL V, fig. 7.
Leaf subcoriaceous, narrowly ovate-lanceolate, equally gradually tapering
from the middle upward to a point and downward to a sJiort petiole, sharply
equally dentate; nervation pinnate, simple, craspedodrome.
Dryophyllum (quercus) salioifolium, sp. nov., PI. VIII, fig. 2.
Leaf linear lanceolate, rounded to tlie base; borders acutely denticulate^
with small teeth turned outward in the lower part, upward in the upper part,
lateral veins numerous, parallel, subcamptodrome.
The fragment represents a slightly falcate leaf, rather membranaceous
than coriaceous, with a narrow middle nerve and close parallel second-
aiy veins, most of them ascending to the teeth and passing under the
sinuses by an upper branch, or some of them curving along the border
and reaching the teeth by a small division. The areolation is not dis-
tinct; only in the upper part of the leaf the nervilles, in right angle to
the veins, appear ramified in the same way, ending in square or polygo-
nal areolae.
This species is comparable, and, indeed, closely related to Dryophyllum
lineare, Sap., Sezane flora, p. 350, PI. IV, hg. 6.
Habitat. — Near the San Juan Biver, at a higher Cretaceous station
than the Dakota group. Southwest Colorado, W. H. Holmes.
Quercus hexagona, Lesqx., Cret. Flor., p. 61, PI. V, fig. 8.
Leaf rhomboidal ovate, tapering from above the middle to an acute pointy
varrowed,wedgeform to the petiole, irregularly broadly dentate in ike upper
part only, nervation pinnate, simple croAspedodrome.
Quercus ? ellsworthiana. Lesqx., Cret Flor., p. 65, PL VI, fig. 7,
Leaf subcoriaceous, oblong oval, point brolcen, narrowed in a curve to the
base; borders undulate; nervation pinnate, camptodrome.
The relation of this fragment is as yet uncertain.
iJEsiiUKRKux.] ENUMERATION OP CRETACEOUS PLANTS. 341
QUBBGUSt POBANomES, Lesqz., Gret Flora, p. B6, PL XXX, fig. 9.
Iieaf brooMy oval or nearly rounds point brolcenj truncate at t-he hase^ uth
duiate on tJie borders^ middle nerve thickj lateral veir^ ihin^ aubopposite^ at
an open angle of divergence^ curving to and along tlie borders^ camptodrome.
The reference of this fragment is as uncertain as that of the former.
Fagus polyolada, Lesqx., Oret Plor., p. 67,»P1. V, fig. 6.
Leaf ovate^ oblong^ cuneate to the base^ short petioled; borders entire^
undulate; middle nerve straight^ secondary veins closcy numerous j simple^
parallel and craspedodrome.
PLATANEiE.
PL.ATANUS OBTUSi LOBA, Lerqx., Cret. Plor., p. 69, PI. VII, figs. 3, 4.
Leaves smaU^ not thick^ palmately irregularly trilobate; lobes obtuse^ short
toith regularly undulate borders^ nervation 3 to 5 palmate from a distance
above the base of the long petioled leaf
Platanus primjera, Lesqx., Cret Flora, p. 69, PI. VII, fig. 2, and PL
XXVI, fig. 2.
Leaves large, coriaceous^ palmately trilobate, tciih short, scarcely dis-
tinct lateral lobes, broadly deltoid, deeply, distantly dentate to the point;
nervation three palmate, coarse^ platanoidal,
Platanus Heerii, Lesqx., Cret. Flora, p. 70, PL VIII, fig. 4, and PL
IX, figs. 1 and 2.
Leaves round or broadly rhomboidal in outline, palmately three obscurely
lobed; lobes shorty obtuse ; borders entire or undulate broadly wedge form
at base and more or less decurrent to the short petiole.
We have of this fine species a specimen representing a small leaf
nearly entire on the border and with the trilobate form scarcely defined.
The supposition tbat these leaves coald be referable to Credneria is
contradicted by the short petiole, besides the other dififerences indicated
in the introduction.
Platanus I^ewberriana, Heer, Cret Flora, p. 72, PL VIII, figs. 2, 3;
PL IX, fig. 3.
Leaves of medium size^ thicHsh, palmately three lobed, either tapering
to a point from the lateral lobes uptcard, orwitltout lobes and ovate ; taper-
pointed, broadly cuneate to the base, equally dentate / nervation trifidfrom a
little above the base ; secondary veins close, numerous.
Platanus diminutiva, Lesqx., Cret Flora, p. 73, PL VIII, fig. 5.
Leaf small, thick, half round from the middle to the base, narrowed to an
obtuse point ; borders entire^ undulate ; nervation trifid from above the
base; nerves thick and irregularly inflated.
As remarked already, this may be a diseased leaf of one of the for-
mer species.
URTICINEiE. MORE.^.
Ficus Halliana, Lesqx., Cret. Flora, p. 68, PL XXVIII, tigs. 3 and 9.
Leaves siibcoriaceous, very entire petioled, broadly lanceolate, gradually
narrotced to a long acumen, more rapidly narrowed and rounded to the
petiole, 7te>'vation pinnate; lateral veins close, straight on an acute angle
of divergence, parallel, nutnerons.
342 GEOLOGICAL SUUVEY OF THE TEHRITOBIES.
FiCUS LAUROPHYLLUM, sp. nov. PI. V, fig, 7.
LaurophyUum reiiculatuvif Lci^qx., Cret. Flora, p. 7(), PI. XV, liga. 4,5.
Leaves coriaceous^ entire narrowly lanceolate acuminate^ gradually taper
ing to a shorty thick petiole; nervation pinnate, middle nerve thicky grooved,
secondary veins close, open,
A large uuinber of fipecimens have been obtained of this fine s|ie-
cies. Though generally more or less fragmentary, they indicate, by
comparison, the essential characters of the leaves. They vary in size
from one and one-half to four and one-half centimeters broad in the
middle, and from ten to eighteen centimeters long. Their form is like
tbat of PI. V, fig, 7, of this memoir, which is an exact likeness of the
only leaf seen preserved in its whole. The secondary veins are always
open, nearly at a right angle to the very thick, broad, and grooved or
rather channeled middle nerve. The areolation is by tibrillae at
right angle to the secondar}' and intermediate tertiary veins, forming
irregular quadrate or- polygonal loose meshes. The secondary* veins
carve along the borders, and, connecting with those above, form a kind
of margin, very undistiuct, however, to the leaves. These characters ot
nervation and areolation more evidently refer this species to the FieuM
than to any division of the Laurinece. They are the same as in the
leaves described as Fious protogcce, Ileer, in Flora Arct. Ill, p. lOS, PL
XXX, figs. 1-8 of the Upper Cretaceous of Greenland. Some living
species, especijilly of Cuba, have the same type of nervation and areo-
lation. The relation of these leaves is also marked to 8i)ecies of Nerium,
Ficus DiSTOBTA, sp. nov., PI. V, fig. 5.
Leaf coriaceous, entire, obovate, unequilateral, pointed or acuminate,
apparently gradually narrowed to the base (broJcen); nervation pinnate,
secondary veins thick, parallel, equidistant camptodrome; nervilles in right
angle to the veins, areolation irregularly quadrate or polygonal.
This fragment as figured here is the only one seen of this species, and it
is not sufficient to positively indicate the relation of the species to Ficus;
the unequilateral shape of the leaf, its nervation and areolation seem to
authorize its reference to this genus.
Habitat. — Near Fort Harker, Kansas, Chs. Sternberg,
LAURINEJi:.
Laurus Kebrascensis, Lesqx., Cret. Flora, p. 74, PI. X, fig. 1, PI. XXVIII,
fig. 14.
Leaves Hiick, coriaceous, elliptical oblong or narrowly lanceolate, obtufeUf
potnted, tapering doxcnward to a short, tJdcJc petiole ; middle nerve thick,
half round; secondary veins alternate, at an acute angle of divergence, camp-
todrome.
IiAUBUS macrocarpa, Lesqx., Cret. Flora, p. 74, Pl.X, fig. 2.
Fruit round, oval; nut surrounded by a thick pericarp; pedicel divb-
sliaped.
The fruit may belong to the species represented by the leaves of
Laurus Nebrascensis.
Laubus PROTE-asFOLiA, sp. nov., PL V, figs. 1 and 2.
Leaves subcoriaceous, broadly lanceolate^graduaXly narrowed from btloffi
the middle into a long acumen, more rapidly narrowed to the base ; middle
nerve narrowly groovedand comparatively narrow; lateral veins obligue, slen-
der j curving to and along the borders, parallel, except the lower pair, which
is more oblique and ascends higher.
iJtaQUKREUx.] ENUMERATION OP CRETACEOUS PLANTS. 343
These leaves, of which we have a number of specimens, the two best
ones figured here, vary iu size from two to three and one-half centime-
ters broad in the widest part, far below the middle, and twelve to six-
teen centimeters long. By their shape, the long narrowly tapering and
slightly falcate acumen, they closely resemble F-roieoides dafhnogeiioides,
Heer, as represented in Oret. Flora, Pi. XV, figs. 1 and 2, differing,
however, by the brdader middle nerve and the distinct, equidistant and
jiarallel secondary veins. These, at an acute angle of divergence of
ii bout thirty degrees, are somewhat curved in passing toward the bor-
tiers, where they become effaced ; the lower pair is at a more acute angle
of divergence and ascends higher in following the borders; the areola-
tion is obsolete, the surface appearing punctulate or closely dotted by
bniall convex areolae, like the leaves of some species Laurus or Persea.
Habitat. — Near Fort Harker, Kansas, Chs. Sternberg.
Persea Leconteana, Lesqx., Cret. Flora, p. 75, PI. XXVIII, fig. 1.
Leaf large, oblong-ovatej lanceolate pointed ; borders undulate, nervation
pinnate; lotcer secondary veins distant, at a more acute atigle of divergence,
curving near the borders and ascending to the middle of the leaves ; upper
reins shorter, parallel.
The character of the nervation is the same as in the former species.
The relation of this leaf is, however, contested, on account of its size
and shape, which seem more like those of a Magnolia.
Persea Sternbergii Lesqx., Cret. Flora, p. 76, PL VII, fig. 1.
Leaf large, thick, coriaceous, entire, broadly oblong, oval, or obovatc,
obtusely pointed f f point broken), gradually narrowed in a curve to the base ;
nervation pi,nnate, very distinct, camjptodrome.
Daphnogene oretacea, sp. nov.
Cinnamomum Scheuchzerij Heer, Crot. Flora, PI. XXX, figs. 2, 3.
Leaves co^Haceous, polished on the upper surfa^^e, elliptical or ovate-lanceo-
late, pointed, narrowed to a short petiole; slightly undulate on the borders,
and triple-nerved from a distance above the base ; middle nerve and lateral
reins thick, the lotcer primary ones ascending along the borders as high as
the lo-wer secondary veins, which they join by ramifications.
To Professor Heer, the reference of these leaves to Cinnamomum
Schenchzeri seems very hazarded, for though the form of the leaves is
much the same, the middle nerve is too thick for that species, especially
toward the point. Count Saporta is also of the opinion that the presence
of C. Scheuchzeri in the Cretaceous is very improbable, as this species in
Europe is essentially of the Upper Miocene. I have accordingly changed
the name of this species, which, though positively referable to the
LaurinecB, is as yet uncertain in its relation. The genus Daphnogene,
Ung., less definitely limited^ is appropriate for leaves of this kind, to
which the following species is also referred. These two leaves are dis-
tantly related to Cinnamomum Mississippiense of the lignitic.
Daphnogene heerii.
Cinnamomum Heerii, Lesqx., Cret. Flora, p. 84, PI. XXVIII, fig. 11.
Leaf thickish, subcoriaceous, entire, ovate, taper-pointed, rounded at the
base, three-nerved ; lateral veins ascending higher than the middle of the
leaf, branching outside.
Obeodapdne cretacea, Lesqx., Cret. Flora, p. 84, PI. XXX, fig. 5.
Leaf coriaceous, elliptical, gradually curving to an obtuse point, narrowed
in about the same degree to the base; middle 7ierve thick, secondary veins
thick and opposite^ three or four pairs, inflated at the axils.
344 GEOLOGICAL SURVEY OF THE TEBBrrOBIES.
SASSAFftAS.
The remarks Iq the introd action expose the opinions of paleontologists
and the discussion upon the species referred to this generic diviaion
from the specimens of the Dakota group. They prove that, though the
number of these leaves is very large, their generic reference is still very
uncertain. Leaving aside for the present the task of deciding on the
evidence in regard to the degree of their relation to Sassafras or Aralia,
I shall here describe them provisionally under the generic name of Sas-
safras and Sassafras {Aralwpsis)^ placing this group altogether at the
end of the Laurinew until we get some more positive information oa the
subject.
Sassafras Mudgbi, Lesqx., Cret. Flora, p. 78, PL XIV, figs. 3, 4; PL
XXX, fig. 7.
Leaves proportionally long ; primary nerves narrow j at an acute angle of
divergence; middle lobe tfcice as long as the lateral one; all ovcUe'laneeo-
late obtusely pointed ; base of the leaves narrowed^ acutely cuneate to ^e
petiole; surf ace of the leaves polished.
Sassafras acutilobum, Lesqx., Cret Flora, p. 70, PL XIV, figs. 1, 2.
Leaves svhcoriaceous^ of the same consistence as the former species; lat-
eral lobes lanceolate, sharply pointed, entire^ middle lobe twice as long as
the lateral ones^ which diverge nearly at right angle ; base of the leavat
narrow and tapering.
The leaves of this and the former division are rare among the speci-
mens furnished to me. This so-called species is perhaps a variety of
the former. Both were found at the same locality.
Sassafbas (Abaliopsis) gbetageum, Sewby., Oret. Flora, p. 80,
PL XII, fig. 2.
Leaves comparatively of small size, icit/i diverging^ obtusely pointed^ short
lobes, enlarged toward the broad sinuses ; broadly cuneiform^ and decur-
ring to tlie raohiSj longpetioled; border entire.
Vab. dentatum, Cret. Flora, PI. Xi, figs. 1, 2.
Differs by the lobes more or less dentate on the borders^ and the secondary
veins subcamptodrome or mixed.
Sassafbas (Abaliopsis) cbetageum obtusum, Lesqx., Cret Flora,
p. SO, PL XII, fig. 3, PI. XIII, fig. 1.
Leaves of various size, some of them very large, with short obtuse entire
lobes, the lateral diverging in an obtuse angle and the nervation coarse and
very deep.
From a number of specimens examined, this form appears truly dis-
tinct by its peculiarly broad nervation. Even in the smallest leaves tbe
primary nerves are twice as thick as in the leaves described as Sassafras
cretaceum. This character is well marked upon fig. 3 of PL XII espe-
cially. It cannot be considered as a modificatiou resulting from tbe
different face of the leaves preserved by the specimens, as some of these
in the collection are double specimens, representing both faces, where
the same difference is distinctly remarked. I have also not seen any
leaves of this coarse nervation with denUil borders ; the lobes are always
entire. To this division are referable some leaves evidently of the same
type, but entire, or not lobed. One of them has been described in Ore-
tiiceons Flora as Sassafras? subinteyrifolium, p. 82, PI. Ill, fig. 5, which
is apparently abnormal or distorted by compression. A number of better
s|)ecimens represent leaves of this kind nearly entire or broadly oval, with
one obscure lobe on one side, or none, and the deep, coarse, broad nerva-
J
ussQUEMux.] ENUMERATION OP CBETACEOUS PLANTS. 345
Hon which is a character of this so-called variety. I will further remark
that specimens of both the entire and trilobate leaves were found at
the same locality.
Sassafras ( Abaltopsis) hirabile, Lesqx., p. 80, PI. XII, fig. 1.
Ijeaves thickj coriaceotts, large ; lobes broad and shorty the lateral ones on
a broad angle of divergence, with borders dentate or deeply, undulately lobed ;
neoondary veins mostly craspedodrome.
A remarkable modification of the character of this species is observed
TipoD a fine leaf still much larger than the one figured in the Cretaceous
Flora. It is twenty centimeters broad between the points of the lower
lateral lobes ; about fifteen centimeters long from the top of the petiole
(lower part of the leaf destroyed), divided by the forking of the lateral
primary veins in five equal ahd equally sinuate dentate lobes, with the
same character of nervation as in the normal form. The lobes also are
of equal length and width ; the middle one fifty-seven millimeters broad
and scarcely sixty millimeters long, with the lower secondary veins
camptodrome and the upper ones/craspedodrome, and entering the teeth.
As 1 have remarked it already, this subdivision in four lobes tends to
show the reference of those large leaves to Aralia rather than to
Sassafras. But it may be also an exposition of that disposition to poly-
morphy so remarkably evident in the leaves of our living Sassafras offi-
cinale. As these generally tripalmate leaves pass to an entire oval shape
sometimes, they subdivide more or less in the same way. One of the
largest specimens of S. mirabile, lately received from Mr. Towner, of
Clay Center, Kansas, has one of the lateral primary nerves twice as
thick as the other, and its base is higher. One of its lobes is, therefore,
much longer, fifteen and one-half centimeters, while the other is only ten.
Sassafras, (Araliopsis,) reourvata.
Platanus reourvata, Lesqx., Cret. Flora, p. 71, PI. X, figs. ^-5.
Leaves three to five palmately lobed; hbes nearly equal in length, the mid-
dle one broader^ lateral nerves curving downward, simple or forking above
the base; borders of the lobes entire or sparingly coarsely dentate.
This form is still more uncertain, and, so to say, transient in its char-
acters. By the decurrent base of the leaves descending to the petiole,
lower than the point of union of the primary veins and also by the trilo-
bate division, it is a Sassafras. The irregularity, however, of the lobes,
the nervation and the double divisions in lobes or teeth refer it to Plar
tanus; the tendency to become five-lobate by the forking of the lateral
iierve)» is a character of the AraliacecB. This disposition to a subdivis-
ion or multiplication of lobes is seen in fig. 3, where the lower branches,
though thick, do not diverge widely enough tor modifying the borders
of the leaf, but are curved inward and join the secondary veins at the
base of the lobes ; but in fig. 4, which represents a fragment only, the
subdivision in five lobes is evident. It is still more marked upon a leaf
recently found and figured by Mr. H. C. Towner. lu this one the cnneate
base of the leaf descends far down, two and one-half centimeters lower
than the poiut of union of the primary nerve ; the lateral ones divide
in two branches from below the middle, and curving backward they form
well defined ovate pointed short lobes, and thus a palmately five-lobed
leaf of the Aralia type. This leaf, without the petiole, which is broken,
is twelve centimeters long, and as wide between the points of the lowest
lateral lobes, which are only one and one-half centimeters long ; the oth-
ers, as also the middle one, are three centimeters long and about as
wide, being half round, cuspidate, and separated by narrow obtuse si-
nuses.
346 GEOLOGICAL SURVEY OF THE TEBBITORIES.
PROTEAOE^.
LOMATLLt SAPOBTANEA.
TodeaY Sapobtakea, Lesqx., Cret Flora, p.489 PL XXLX, figs. 1-4;
PL VI, fig. 2 (enlarged).
Leaves coriaceous^ pinnately laciniate; divisions entire^ narrowly lan-
ceolate^ pointed^ connected by the decurring basCy tchick forms a more or le^
broad and nerved tcing to the rachis; primary veins thicJc^ ascending to the
point ; secondary veins distinct, at an acute angle of divej'gence, close^ par-
allel^ curving up in passing to the borders and following them in simple fes-
toons; areolation mixed by tertiary veinlets and their branches in various
angles of divergence.
The fine specimens figured in the Cret. Flora, as quoted above, repre-
sent the essential characters of the leaves; the branches parallel and
distichous? along the primary stems, a disposition similar to that of
the fronds of a number of species of large ferns by parallel open pinns.
The point or upper part of three of these dissected parall^ leaves is
represented in fig. 1; this division is by more or less distant segments,
which, opposite or nlteruate, are of various size, narrowly lanceolate
pointed, decurrent at the base, and thus connected by a wing along the
rachis. As seen at the base of the segments of the middle leaflet of
fig. 1, the wing along the borders is nerved like the divisions or leafietn.
The middle vein of these segments is thick ; the secondary veins close,
parallel, turned up in passing to the borders, simple, but joined in vari-
ous directions by oblique nervilles, forming a mixed, angular, square,
or polygonal areolation. The nervation and areqlation were exactly
copied for fig. 2 of PL YI of this memoir, but the wood-cut does not
expose it in its details. Some of the specimens show the upper part of
three parallel leaves whose tops are on a right line and more exactly
like the upper pinnte of a fern than the specimen figured in the Cret.
Flora.
My first opinion in regard to the relation of these remarkably fine
vegetable remains was that they represented some kind of an old ex-
tinct type of Filices. I even supposed that, considering the peculiar
disposition of the leaflets and their nervation, we had here something
like a transient form between the ferns and plants of a higher order. The
sections of the leaves are similar to those of some species of fossil ferns,
Stenopteris desmomera^ Sap.,* for example, which, from the remarks of the
author, is without relation to any living fern ; also like the fragment
described by Debey and Ettiughausent under the generic name of Jfon-
Jieimiay which not only have a similar division of leaves or pinnae, but,
as seen in fig. 6, a nervation of an analogous character, the numerous
parallel secondary veins curving up along the borders, some of tbein
united by oblique veinlets. A mere sketch of one of my specimens sent
to Count Saporta gave him the same impression in regard to its refer-
ence to ferns. But the areolation was not represented upon it, and the
characters of the areolation especially remove the species to another
order of vegetables, the Froteacece, indeed species of Lomatia have the
leaves pinnately laciniate, with the divisions^lternate, decurring along
the middle nerve or rachis, and a nervation and areolation somewhat com-
parable to those of the fossil species. I have therefore abandoned the
first reference, and, following the opinion of the celebrated author from
* Plantes fosstles des Itts de poissons de CeriD, by CoaDt Saporta^ p. 82^ PI. XIV.
tUrweltlicben Acrobryen, p. 33, PI. IV, figs. 1-10.
ij»QLiJSF.ux 1 ENUMERATION OF CRETACEOUS PLANTS. 347
wbieli this species is named, T have placed it with the Proteacece. I am,
however, still iincertaia in regard to the trae relation of these remarka-
ble remains. There is, as said above, in the position and the subdivis-
10D8 of the leaflets a remarkakle afiinit.y with those of some species of
ferns, and at the same time a discrepancy with what is remarked in the
segments of the leaves of Lomatia and other species of laciniate Pro-
teacecD, In the fossil plant the decurrent base forming a wing of the
rachis, has the same character of nervation as the leaflets, while in the
basilar segments of the Proteacece the winged part is generally without
visible veins, or rather veined lengthwise. Moreover, there seems to be
a kind of anomaly in the presence of plants of the so called Australian
types in a vegetable group where the characters of the present American
flora are so predominant, or in connection with species of Fagus, Lyrio-
dendrofiy Plaianus^ etc. The leaves described ander the name of Prote-
oides are as yet not positively referable to the ProtecLcece^ their nervation
being still unknown ; and thus we should have to admit this Lomatia t
as the only representative of an Australian type among a large number
of forms of different afiinities.
This species has been found originally in very fine specimens by Prof.
B. F. Mndge, in Southern Kansas. I have lately received a small frag-
ment only from Mr. H. 0. Towner, found near Clay Center, ELansas.
Proteoides daphnogenoides, Heer, Cret. Flora, p. 85, PI. XV,
figs. 1, 2.
Leaves ovate-lanceolate toward the base, gradually tapering upward to a
long scythe-shaped acumen^ entire^ smooth and coriaceous; middle nerve
narrow ; secondary veins obsolete, feWj ascending at a very acute angle from
the middle nerve and following the borders.
Proteoides acuta, Heer, Oret. Flora, p. 86, PI. XV, fig. 3:
PL XXVIII, fig. 13.
Leaves ooriaceousy linear lanceolate^ narrowed to the base and gradually
so to a scytheslwped point ; borders undulate ; middle nerve strong^ sec-
ondary veins obsolete,
Proteoides greville^formis, Heer, Cret. Flora, p. 86, PI. XXVlir,
tig. 12.
Leaf coriaceous^ small^ enlarged above tlie base, litiear-lanceolatefflexuous;
borders entire ; middle np^e thick ; secondary veifis alternate^ thin, aero-
drome, ascending nearly parallel to tJie borders and slightly curving
inward.
EMBOTHRiTESf DAPHUiBOiDES, Lesqx., Cret. Flora, p. 87, PI. XXX,
fig. 10.
Leaf coriaceous, polished, oblong, narrow, gradually narrowed downward
and decurrent to the enlarged middle nerve; borders slightly reflexed ; nerva-
tion pinnate; lateral veins opposite, close^ at a very acute angle of dicer-
gence.
This fragment of leaf is of an uncertain attribution.
AS^VRINE^.
Aristolochites dentata, Heer, Cret. Flora, p. 87, PI. XXX, fig. 6.
Leaf nearly round, thickish, split from the base of the petiole to the
borders, undulate-crenate, three-nerved; secondary veins curving and anas-
tomosing in large, oval^ angular mesJics.
318 GEOLOGICAL SURVEY OF THE TERRITOKIES.
GAMOPETALE^.
BI00BI7ES.
Ai9DB03iEDA PABLATOBii, Heer, Cret. Flora, p. 88, PI. XXIII, figs. C-7;
PI. XXVIII, fig. 15.
Leaves lanceolate, narrowed to the base and decurring dUmg the petiole ly a
narrow border^ entire; middle nerve thick; secondary veins at an acute
an-gle of divergence^ parallel^ camptodrow£,
Andbomeda affinis, sp. Dor. PI. Ill, fig. 5.
Leaf thickish, narrowly lanceolate^ narrowed to a long acumen^ gradually
decreasing toward tlie base / borders entire ; middle nerve comparative
thick; lateral veins close, parallel^ subequidistant, in an acute angle of
divergence ; areolation minute.
The leaf fire and one-balf centirr.elers long, eleven millimeters broad
in its widest part, the middle, is gradually equally narrowed down to
the petiole and up to a long narrow acumen, and entire ; the secondary
veins are numerous, simple, at an angle of divergence of 30^, parallel,
rather obsolete, though thickish, scarcely curving in ascending close to
the borders, camptodrome; the areolation is in round or quadrate- polyg-
onal minute areolae. It is closely allied to the former species, if not a
variety of it.
Habitat. — Spring Cafion, where it is mixed with fragmentary leaves
of Andromeda parlatorii; the horizon of this locality is not geologically
determined, Dr. F. V. May den,
DiosPYBOS AMBiGUA, Lesqx., Cret. Flora, p. 89, PL VI, fig. 6.
Leaf coriaceous, narrowly oval, narrowed mear tJie point into a short
slightly obtuse oAyiimev. ; borders entire ; nervation pinnate^ camptodrome.
DiosPYBOS BOTUNDIFOLIA, Lesqx., Cret. Flora, p. 89, PI. XXX, fig- 1.
Leaf subcoriaceous entire^ nearly round, pinnately nerved; secondary
veins parallel, camptodrome; surface undulate, polished.
POLYPETALBiB.
Uhbelliflob^.
Abalia tbipabtita, spec, nov, PI. I, fig. 1.
Leaf small, three palmatcly divided to two-thirde of its length ; lobes
equal, linear obtuse, entire; secondary nervation obsolete.
The leaf is seven centimeters long, six centimeters wide between the
points of the lobes, which diverge in an angle of 25^; cnneate to the
base, which apparently descends a little lower than the |)oint of union
of the primary veins, where it is broken ; lobes four and one-half centi-
meters long, one centimeter broad, nearly exactly linear, abruptlj'
rounded at the point, with perfectly entire borders and obtuse sinuses;
primary nerves thin but distinct, secondary veins totally obsolete. The
surface is smooth and the consistence of the leaf coriaceous.
This small leaf appears like an original simple representative of a type
of Aralia predominant in numerous diversified forms in the Dakota
group.
Babitat. — Near Fort Harker, Kansas, Clis. Sternberg,
ufflQUEKEuxl ENUMERATION OF CBETACEOUS PLANTS. 349
^BALIA CONCBETA, spec. Dov. PI. IV, figs. 2, 3, 4. Cret. Flora, PI.
XXIX, figs. 8, 9.
Leaves small^ very thick j coriaceonsy palmately five-loted to below the
middle^ cuneate and curving to the petiole; very entire; primary veins
threej from the top of the petiole or from a little above the border ba^se of
the leaves^ the lateral ones forking ; all thick j flat j and deep, preserving ilic
Matne size to the top of the pointed lobes*
These leaves vary in diameter from five and one-half centimeters
to eight, across the point of the lobes, not as long as broad ; coneate
to the thick petiole, which they reach by a more or less abrupt carve ;
divided to below the middle in three to five eqnal oblong lanceo-
late-pointed or obtnsely-pointed lobes, separated by narrow sinnses
and very entire. The primary veins are very thick and flat, the lateral
<Hie8 forking above the point of union, as it is the case in all the forms
of this type; the secondary nervation is totally obsolete, as in the
former species. This, however, differs from it, not only by the subdi-
vision in five lobes, but also by the remarkably broad middle nerve.
I had originally separated as a different species, the leaf, fig. 4, under
the name of Aralia semiorbiculata^ on account of its remarkable half-
round base ; of the difference of size of some of the lobes and of the
acute sinuses. As the primary nervation is the same and the secondary
one as obsolete as in the other leaves, the coriaceous consistence being
also a common character, I regard it as probably a mere variety. This
appears the more rational, as all these leaves come from the same locality.
Habitat.— Clay Center, H. C. Towner.
Abalia Townbbi, spec. nov. PI. IV, fig. 1.
Leaves large, coriaceous with polished surf ace, five-Ubed to below the mid-
dle; lobes oblong, obtuse, or obtusely pointed^ entire; primary nerves three
from the top of the petiole, the lateral ones forking above the Imse; second-
ary veins on an open angle of divergence, camptodrome.
This fine leaf of which a part only is figured, is, as seen from another
specimen, fifteen centimeters long, from the top of the petiole, and
twenty to twenty-four centimeters broad between the point of the lobes
which, descending much lower than the middle, are seven to ten centi-
meters long and three to three and one-half centimeters broad. The
primary nerves are comparatively narrow, not l\^lf as thick as in the
former species and gradually narrowing to the point ; the form of the
lobe is oblong, the point slightly obtuse, the sinuses also obtuse. The
secondary veins, distant and on an open angle of divergence pass toward
the borders in curves and follow them in festoons, anastomosing by nerv-
illes with those above; they are generally separated by tertiary shorter
veins, forming by their ramifications in more or less oblique directions
square or polygonal angular large meshes. Though the general out-
line and the division of tbese leaves are similar to those of the former
species, they evidently differ, by narrow, primary veins, less coriaceous
substan<^ polished surface, and distinct areolation. The type is, how-
ever, the same.
Habitat. — Same as the former, JT. C Towner.
Abalia quinquepabtita, Lesqx., Cret, Flora, p. 90, PL XV, fig. 6.
Leaves membranaceous, three-nerved from a distance above the base; five-
lobed by fAe forking of the lateral primary nerves; lobes oblong or oblance-
olate^ somewhat narrowed downward, distantly dentate toward the point;
base of the leaves deltoid cuneiform*
We have now of this species, described in the Cret. Flora from a mere
fragment, a far better specimen. It represents a leaf sixteen centime-
350 GEOLOGICAL SUEVEY OF THE TERRITORIES.
ters long from the point where the base joins the petiole to the top of a
large lateral Idbe preserved in lull ; its base narrowed in a carve, and
deenrrent. It is deeply divided in six narrow oblanceolate lobes nar-
rowed toward tho sinuses, dentate from the middle upward, the lower
lateral ones nearly entire ; the middle ones twelve centimeters Iod^,
two centimeters broad in the middle, and only one centimeter near the
sinuses. The distance between the points of the external lobes is nine
to ten centimeters. The primary lateral nerve on one side forks twice
and .therefore forms three divisions or lobes, while on the other side it
forks once only, and therefore has two divisions, and thas the leaf is
six-lobed, though the normal division of the leaves is by five. Thoa|^
thickish, they are of a rather membranaceous consistence and smooth.
The lateral veins, though obsolete, appear very thin, diatribated aboat
as in the following species, but on a broader angle of divergence aod
more curved in passing up to the borders. From the base of the lobes
downward no trace of nervation is observed.
Habitat. — Near Fort Harker, Kansas, C/«. Sternberg,
Aralia saportanea, sp. nov. PI. I, figs. 2 and 2».
Leaves palmately Jivelobed to above the middle^ narrowed in a curve or
broadly cuneate to a long^ slender petiole^ fan shaped in outline; lobes of
different size^ lanceolate^ obtusely pointed^ distantly dentate; nervation
craspedodrome.
The leaves are variable in size, from nine to eighteen centimeters loog
without the petiole, and from nine to twenty centimeters broad between
the points of the external lobes ; lobes lanceolate, gradually taperiug to
an obtuse point, distantly obtusely dentate; the lateral ones grada^Iy
shorter than the middle one, which, in the largest of our specimens, is
twelve centimeters long from the point to the obtuse sinuses; leaves
three-nerved from the base; lateral nerves forking once, and lateral
lobes oblique at an acute angle of divergence. The nervation and areo-
lation are perfectly distinct in all the specimens, and its characters
identical ; the secondary veins, at an acute angle of divergence of thirty
degrees, curve in passing up to. the borders, where they enter the teeth,
and are then craspedodrome, while the lower ones more generally follow
the entire border base of the lobes ; the nervilles are strong, nearly
continuous, branching at right angle, and forming by this kind of divi-
sion small square or equilateral areolse.
The leaves which represent this species are of a beautifal and elegant
pattern ; the small ones still more finely shaped by the distribution of
the lobes, which are acutely i)ointed, and at a more open angle of dis-
tribution toward each other. They represent,'* perhaps, a diflFerent
species; but I could not find a persistent and distinct character, neither
in the form nor in the nervation, to separate them. By the texture,
which though thickish is not membranaceous, by the form of the
broader lobes not narrowed toward the sinuses, by the distinct nerva-
tion, the point of union of the primary nerves at the non-decurrent base
of the leaves, the species is evidently different from the former, though
found at the same locality. The relation of these Aralia leaves to the
Sassafras {Araliopsis\ especially to S, mirahUSy is easily remarked;
there is, however, a great difference in the characters of nervation and
areolation, clearly perceivable in comparing our fig. 2^ with the leaves
in Cret Flora, PI. XI, fig. 1, and PI. XII, fig. 1. The habitat of these
Aralia species shows once more the peculiar grouping of leaves of
same or analogous characters in a same locality. Aralia quinquq^tita
and A. Saportanea are from the south of Fort Harker, Kansas, while the
ijaiQURRKLx.l ENUMERATION OF CRETACEOUS PLANTS. 361
two species with entire loaves, A. Toicneri and A. concrcta^ were fonnd
near Claj* Center, except A. tripartita^ which al«o is troin Fort Barker.
These tive new types of (Jretaceoas plants proves the richness of this
remarkable flora, and their local distribution assures for future explora-
tions a rich field for new discciveries.
Habitat. — South of Fort Harker, C/w. Sternberg.
Hedkra ovalis, Lesqx,, Oret. Flora, p, 91. PI. XXV, fig. 3, and PL
XXVI, fig. 4.
Leaves coriaceovs^ entire^ oval^ rounded at the pointy narrowed to
the base^ pinnateJy nerved; middle nerve thicic; secondary veins alternate^
irregular in distance^ more or less numerous ; areolation in large irregular
meshes.
These leaves have an evident relation to those published by Professor
Heer under the name of Chondrophyllum NordensJcioldi and C.orhicufatum^
from the upper Cretaceous of Greenland Foss. in his Flor., Arct., Ill, pp.
114 and 115, PI. XXXII, figs. 12 and 13, reconstructed from fragments.
When the specimens are compared, they may prove to be the same spe-
cies, for, though I have formerly considered the leaves as representing
one species only, for the fragments show a great divermty in the charac-
ters of the nervation, there is, however, too great a difference between
the multiple much-divided secondary veins on a broader angle of diverg-
ence of PI. XXV, fig. 3, and the more simple nervation of PI. XXVI,
fig. 4, to permit considering them as representing the same species.
Hedera Schimperi sp. nov. PI. VII, fig. 5.
Leaf subreni/orm^ broader than long, rounded at the top^ abruptly nar-
rowed or nearly truncate to a short petiole, three-nerved from above the
base; lateral veins curving in various directions toward the borders,
anastomosing by thicic branches and nervilles with the divisions of the short,
distant secondary veins, curving along the borders and entering by short
veinlets the distant^ slightly marked denticulations of the borders.
A fine leaf of coriaceous substance, six centimeters long without the
petiole (which is only seven millimeters long and enlarged at its base),
six and one-half centimeters broad, with borders minutely denticu-
late, the teeth at different distances and of various size, and a trifid
nervation from a short distance above the border base of the leaf; the
lateral veins curve, the one inside toward the middle nerve, the other
outside toward the border and branching nearly at right angle, they anas-
tomose with nervilles or divisions of the secondary veins and form an
areolation irregular and mixed with angular, square, or polygonal
meshes. This areolation partakes of the characters of that of the former
species. It is somewhat analogous to that of Oreviopsis tremulafolia,
and of Cissus ampelopsidea Sap., and recognizable also in the following.
Habitat. — South of Fort IJarker, Chs. Sternberg.
Hedera platanoibea, sp. now PL III, fig. 3.
Leaf small, broadly ovate, truncate at the base, round at the topy short
petioledj entire; nervation trifid from a short distance above the base; pri'
mary veins craspedodrome.
This leaf five centimeters broad, four and oncbalf centimeters long
without the short enlarged petiole, has its borders entire, though
the primary and secondary veins reach to the borders and enter them ;
the two lateral primary nerves force the border slightly outside, and the
leaf appears thus sublobate or enlarged in the middle; the lower branches
352 GEOLOGICAL SURVEY OF THE TEREITOEIES.
of the lateral nerve follow the borders in festoons along the base of the
leaf, and, as in the former species, there is a pair of marginal veinleta
under the primary nerves, and at right angle to the midrib. The areola-
tion is mostly in square or angular large meshes, less irregular than in the
former species. From the form of the leaf, the short inflated petiole, and
the character of the areolation, the leaf appears referable to the same
generic division as the former. It differs, however, by the primary and
secondary veins joining the borders, and not curving inside of them.
These two leaves appear to be transitional in their characters between
the Araliacew and the Ampelidece.
Habitat. — South of Fort Harker, Chs. Sternberg.
AMPELlDEiE.
GissiTES, Heer.
Under this generic name. Professor Heer has described in the PkyU
lites du Nebraska^ p. 20, PI. II, figs. 3 and 4, fragment of a leaf which
seem to have a cloise affinity to those which I describe nuder this same
division. These leaves, enlarged on the sides and above the middle
by the extension of primary lateral veins, are either deltoid, pointed,
or round, or lobate at the top, and broadly rounded and attenuated to
the base. Their primary nervation, trifid from above the base-
border of the leaves, is of the same type as that of the Sas^afroM
(Ara{u;|>m), and the secondary veins, all camptodrome, curving along
the borders in successive bows, have also an undeniable affinity with
the same group. But they evidently differ by the less distinct trilobate
division of the leaves, the broader base, the smaller size, and the general
facies. It is evident, however, in comparing the leaves described under
this generic name, that closely related as they are between themselves,
they are altogether allied by some of their characters to the Aralioea.
CissiTES Habkeeianus. PI. VII, figs. 1 and 2.
Sassafras (Araliapsis) Sarkerianumf Lesqx., Grot. Flora, p. 81, PI. XI, Ag, 4.
Leaves caria^eous^ round in outline, suhtrilobate, broadly cuneate to the
ba'Se'j nervation trifid from above the border base; lateral primary reins
branching outside; secondary nerve simple^ distant, mostly opposite campto-
drome or craspedodrome.
The two leaves figured here are smaller than that of Plate XI, fig.
4, of the Cretaceous Flora ; but there is not any marked difference in the
outline and the nervation; we have, moreover, specimens showing
leaves of intermediate size. The nervation is more or less pronounced,
according to the face exposed by the specimens. This and the following
form might be indifferently referred to Sassafras {Araliapsis) or Cissus,
CiSSITES AFFINIS.
Platanus affinis, Lesqx., Cret Flora, p. 71, PI. IV, iig. 4, PI. XI, fig. 3.
Leaves coriaceous or subcoriaceous, round, polygonal in ouUine, SMhtri'
lobed, rounded and nai^oiced to the petiole, broadly deltoid to the point;
borders undulate; distantly short dentate; nervation trifid from Ae base
or from a little above the borders.
From the comparison of a number of specimens, and especially from
the discovery of one representing, by the splitting of the stone, both
sides of the leaf, I have ascertained that the one represented, Plate IV,
fig. 4, whose veins are thin, and the surface scarcely furrowed by the
US8QUBBSUX.] ENUMERATION OP CRETACEOUS PLANTS. 353
nervation, is of the same species as tbnt of Plate XI, tig, 3, whose sur-
face is deeply out by broad nerves and secondary veins. In ibis form,
the secondary veins are sometimes all craspedodrome, sometimes mixed.
CiSSITES ACUMINATUS, Sp. nov., PI. VIII, fig. 1.
Xeaf deltoid from tJie middle to the acuminate pointy rounded and SMb-
truncate to tiie petiole^ subtrilobate^ entire coriaceous; nervation trifid/rom
tlie base.
This fine leaf, though of the same type as those described under the
two former specific divisions, differs evidently by its form, its entire
borders, and its secondary veins parallel, close to each other, all campto-
drome. It is about eight centimeters long without the petiole, which
was apparently long and slender; seven centimeters broad between the
two points of the primary lateral nerves, where it is enlarged into a
slightly marked acute lobe, and wherefrom it is broadly deltoid to the
acuminate point. Comparing it to the fine small leaf of Sassafras
Mudgei in Cret. Flora, PL XXX, fig. 7, we easily recognize a likeness
of characters in the form and the nervation, which proves also the rela-
tton of this Cissiies to the Sassafras or the Araliaceas.
Habitat.— Near Fort Barker, Kansas, Chs. Sternberg.
CiSSITES Bbeeii, sp. nov. PL VI, fig. 3.
Leaf fan-shaped in outline^ rounded and ctmeate to the base^ enlarged
above Hie middle^ divided in the upper part into five a^cute nearly equal lobes;
nervation trifid from ahove tlie base ; lotcer secondary veins ascending to
the point of the intermediate lobesj the others all camptodrome like their
divisions.
The base of this leaf is destroyed; but its outline is clearly defined
by the border of the preserved part, and the direction of the lateral
primary vein. The leaf broadly cuneate toward the base, is slightly
contracted a little above, and hence is rounding to join the petiole ; the
two lateral primary nerves ascend to the point of a lower acute lobe,
as also the lower secondary veins, appearing, with the middle nerve, like
five branches of a fi ve-lobed fan-Jike leaf. The lobes are equal, separated
by half-rounded sinuses, and acutely pointed. Except that the two
lower secondary veins ascend to the points of two lobes, the nervation
18 of the same type exactly as in the former species. The afiinity of
these two leaves is therefore evident. It is, however, certain that this
one cannot be now compared to Sassafras {Araliopsis)^ nor to Aralia^
and it therefore authorizes the separation of this group, which by its
characters, seen in this last species, is allied to the AmpelideWy espe-
cially to Cisstis.
Habitat. — Near Fort Barker, Kansas, Chs. Sternberg.
CiSSITES CYCLOPHVLLA, Lcsqx.
Poputiies eydophyllafy Heer,— Cret. Flora, p. 59, PI, IV, fig. 5, aod PI. XXIV, fig. 4.
Leaves round, entire^ subcoriaceous^ witJi slightly undulafe borders, round
or truncate to the long slender petiolej nervation subtrifid or pinnate from
the base; lateral veins straight to the borders, craspedodrome, the lowest
branching.
I am not positive in regnrd to the specific identity of the two leaves,
referred to this species. Fig. 5 of PI. IV has the veins on a more acute
angle of divergence, it being less enlarged on the sides ; fig. 4 of PI.
XXIV, has under the lower pair of lateral nerves a thick marginal vein
in right angle to the mid-rib; in both, however, the veins and their divis-
ions enter the borders, and the nervilles, which join them in right
23 H
854 GEOLOGICAL SURVEY OF THE TEBRITORIES.
angle, are thick, nndalate, at eqaal distance, and generally simple. It
has been remarked already, that the characters of the veins, all craspe-
dodrome, favor a separation of these leaves from the genas PapuhUj
though the round form and long slender petiole give them the appear-
ance of poplar leaves.
OlSSITES OBTU6UH.
Sassafraa o&tttffum, Leaqz., Cret. Flora, p. 81, PI. XIII, figs. 2-4.
Leaver thin^ long petioled^ fldbelliformy three^btusely lobedy entire er
undulate an the borders^ broadly ouneate or narrov)ed to the petiole^ three-
nerved from a little above the border base; secondary veins paraUel, camp-
todrome.
If the relation of these leaves to the Araliacea is marked by the thiee-
lobate form and the nervation, their affinity to the Ampelideceis indicated
also by the thinner substance of the leaves, and the long, slender peti-
ole. Like many other Cretaceous leaves, they are of a mixed character,
and their reference uncertain. Except by their thin substance and long
petiole, they are indeed very similar to fig. 4, of PI. XI, of the Cret
Flora, representing Cissites Harkerianus. By the other characters they
relate to the following generic division.
Ampelophtllum, Lesqx.
Leaves ovate or obovate obtuse entire, narrowed to a long petiole or ««fr-
eordate; palmately three-nerved from above the base; nervation craspedo*
drome.
Ampelophylltjm attenuatum, sp. nov. PI. II, fig. 3.
Leaf broadly obovate, enlarged upward from the cuneate base, rounded
at the top, entire, subcoriaceous ; lateral primary nerve from a distance
above the base flexuous, branchifig outside and inside, ascending to the bor-
ders.
This fine leaf is six and one-half centimeters long without the petiole,
nearly six centimeters wide above the. middle, rounded at the top, un-
dulate by the slight protuberance of the veins, three-nerved from a
distance (one centimeter) above the narrowed base, with two pairs of
distant alternate secondary veins, reaching the bonlers like the pri-
mary nerves, either directly or by their branches. Connected by ner-
villes at right angles, and also divided in very oblique veinlets, they
form irregular quadrate large meshes, and pass up in right angle to
the borders. There is under the base of the primary nerves one or two
pairs of marginal veiulets in the same degree of divergence as the other
veins, 40° to 60o.
The form of this fine leaf and its nervation also are peculiar, and of
a character analogous to that of some leaves described under the ge-
neric name of Oreviopsis in the Sezane Flora by Saporta ; there is,
however, a marked difiTerence in the primary nervation and in the
entire borders of the leaves. The two lower pairs of veiulets give also
to this leaf an affinity with Credneria^ and especially with the small en-
tire leaves of Platanus Heerii as figured in this memoir, PI. YIII, fig.
5 ) The secondary and tertiary nervation are, however, of a different
character.
HABiTAT.^South of Fort Barker, Kansas, Chs. Sternberg.
UBSQOEEEuxl ENUMERATION OP CRETACEOUS PLANTS. 355
Ampelophyllum OVATUM.
CellU r W€Ua Lesqx., Oret Flora, p. 66, PL lY, flgA. 2, 3.
Leaves thickish^ membramaceaus, obtuse or truncate at the point, gradually
enlarged toward the trancate or subcordate base, abruptly curving to a long
petiole^ borders entire, undulate three-nerved from the base, secondary veins
two or three pccirsy at a distance from ike primary oneSj all craspedodrome.
These two leaves evidently represent the same species, bat their refer-
ence to this division is not positive. As in the former species, the lower
veins are irregularly divided, the fibrillse distinct, at least in fig. 3, which
has also one pair of marginal vcinlets; the sabdi vision of the veins along
tbe borders is, however, obsolete, though the vetnlets appear to pass up
into them.
Hahamelites Eansaseana. PL VII, fig. 4.
Alnua Kanaoieanaf L^sqx., Cret. Flora, p. 62, PL XXX. fig. S.
Leaves membranaceous, oval or obovate rounded or subcordate to the ba^e^
obtuse^ undulatCy pinnatety nerved; veins parallel, ascending to the borders
in an acute angle of divergence, branching outside, craspedodrome except the
iatoest, which is more open and curving along the borders.
The specimen figured here is more complete than the one described
in the Cret flora. "No traces of denticalation are observable along
the borders, but regular deep undulations, which near the point pass to
obtuse teeth. Except the two lower pairs of veins, all the others and
their divisions reach the borders ; they are parallel, under an angle of
di\'ergence of 4(P, equidistant and deeply marked. In this specimen
the njiddle nerve passes under the border-base of the leaf, which is
rounded; while in the other fragment figured in Cret. Flora, the border
base is cordate, and curves on both sides to the middle nerve.
From the opinion of Saporta, the author of the genns in the Sezane
flora, the reference of these leaves to the Hamamelites appears legiti-
mate.
Habitat. — Fort Barker, Kansas, Chs. Sternberg.
Hamamelites quadrangulabis.
AInitea quadrantfularie, Lesqx., Cret. Flora, p. 62, PI. IV, fig. t.
Leaf subcoria4seous, small, broadly rhomboidal in outlinCj with obtuse
angles ; borders enUrCy undulate^ rounded to a short petiole (broken); nerva-
tion pinnate; veins parallel, cra^pedjodrome,exoeptthe lower pair mere mar-
ginal veinlets.
The leaf, whose areolation is not distinct, has apparently the same
characters of nervation as in the former species, differing merely by its
shape and its size. Though the veins are thicker it may represent the
6ame species.
POLTOABPIC-aS.
Magnolia tenuifolia, Leaqx., Cret. Flora, p. 92, PI. XXI, fig. 1.
Lea/ large, obUmg, rounded upward to an obtuse point t {Jbroken), nar-
rowed in a curve to a short slender petiole ; middle nerve straight^ narrotv;
lateral veins altematej on a broad angle of divergeneCj slendery undulate^
dtfieaeed near the point of insertion to the mtddle nerve.
Magnolia alternans, Heer, Cret Flora, p. 92, PI. XVIII, fig. 4.
Leaves mticoriaceons ovate-lanceolate orelUpUcalj obtusely poitUedy entire
356 GEOLOGICAL SURVEY OF THE TEBRITOBIfiS.
tapering to the petiole; secondary veins numerous^ parallel^ altematdf
shorter and longer^ camptodrome.
The specimen figured in the Gretaceons Flora is poor. Until recently
I bad not seen any better, neitber of this nor of the following ^peeies
Both have been more commonly found iu Nebraska than in Kansas.
Magnolia capellini, Heer, Pbyllites, p. 21, PI. Ill, figs. 5 and 6.
Leaves coriaceous^ broadly otal^ very entire; secondary veins at an acirfc
angle of divergence, curving to the borders, camptodrome.
Specimens referable to this species were received with others of
M.alternans from Mr. Sternberg; they are all more or less undistioct
and fragmentary. The two forms seem to pass from one to the other by
intermediate degrees, especially in the width of the leaves, so that it is
difficult to find the point of separation between them. The State cabi-
net of New Jersey has a large unmber of specimens representing both
species, some of them appearing indifferently referable to the one or to
the other. But here, also, all the specimens are moro or less fragmentary
and indistinct.
LiRiODENDBON MEEKii, Heer, Pbyllites, p. 21, PI. IV, figs. 3 and 4.
Leaves panduriform [violin-shaped), emarginate at the top, bilobate, laha
obtuse, secondary veins branching.
This species is rare in the Cretaceous, at least iu Kansas. This year
I have received, for the first time, a small specimen discovered in that
State by Professor Mudge. The leaf is of a thin texture, oblong in out-
line, short petioled, deeply emargined, the upper part of the leaf being
thus bilobate; lobes oblong obtuse, one centimeter broad, separated from
the lower lobes by an obtuse narrow sinus scarcely four millimeters broad;
lower lobes eighteen millimeters long from the border of the sinus, ob-
long obtuse, diverging nearly at right angle; base of the leaf rounded
to the petiole. Considering that in the leaves of the present Liriodendnm
fulipifera the emarginatiou of the leaves and the lateral lobes are very
variable in size, it is proper to refer this leaf to the species described by
Heer, for, except the length of the lobes, it has the same char-
acters. The small leaf is without the petiole, thirty-eight millimeters
long, and just the same width between the top of the lateral lobes.
LiBiODENDBON INTERMEDIUM, Lcsqx., Crct. Flora, p. 93, PI. XX, fig. 5.
Leaf large, trilobate; upper lobe deeply emarginate-lobed, secondary veins
thin, simple, parallel.
Since the description of this and the following species, published in
18G8, 1 have not found and not received any specimens referable to
them. They would be very acceptable, for we know these fine species
merely from fragments.
LiBiODENDBON GIGANTEUM, LesQX., Cret. Plora, p. 93, PI. XXIII, fig. 2.
Leaf very large, bilobcd; upper lobe deeply emarginate, segments oblong ob-
tuse^ with four parallel secondary veins.
This mere lol>e of a leaf is about twelve centimeters long, and, there-
fore, would indicate a leaf at least twenty-four centimeters broad be-
tween the points of the upper divisions, or nearly one foot broad, and as
long. Liriodendron tulipifera has in favorable localities leaves as largo
as those indicated by this fragment.
Menispebmites obtusilobus, Lesqx., Cret. Flora, p. 94, PL XXV|fi€&
1, 2 5 PL XXVI, fig. 3.— PI. VII, tig. 3.
Leaves coriaceous, large^ broadly deitoidj either shorter ^ nearly round It
f^
LESQUBMux.! ENUMERATION OF CEETACEOUS PLANTS. 357
outline^ or longer^ narrowed to an obtuse pointy peltate from near the base^
subtrilobate^ fivepalmately nerved^ deeply ungulate.
The fig. 3 of PL VII of this memoir has been given here on account
of the good preservation of the leaf clearly exposing the characters of
tbe genus. Comparing it with the figures of the same species in the
Cret. Flora, its characters appear evidently identical. From tbe large
leaf, fig. 1, PI. XXII, it differs in no manner whatever except by its size,
sbowing, therefore, that this fine leaf is, as remarked, a mere variety of
the normal form. But more than this, by comparison of the distribution
of the veins and of the essential characters of the nervation in the fol-
lowing species, it proves their relation to this generic division, which
has two definite sections,' represented one by lobate, the other by en-
tire leaves.
Habitat.— Clay County, H. C. Toumer.
Mbnispebmites Salinensis, Lesqx.,Cret. Flora, p. 95, PI. XX, figs. 1, 4.
JLeaves tkwkiah, membranojceous or aubcoriaceons, triangttl^xr in ontline^
deeply undulatelobed^ or palmately five-lobed from the border base^ which is
enlarged and truncate,
Menispebmites agebifolius, Lesqx., Cret. Flora, p. 9G, PI. XX, figs.
2 and 3.
I/eaves smaUj triangular in outline^ palmately obtusely threelobedj wedge
fonn^ or abruptly narrowed to the base / nervation three-palmate.
Menispebmites populepolius, sp. nov. PL V, fig. 3.
Leaf broadly ovatCj obtuse^ subcordate at the base^ five-palmately nerved
from tlie border base^ primary nerves in an open angle of divergence^ dividing
an the lower side^ like the secondary veins^ all camptodrome.
The leaf is broadly ovate, perfectly entire, coriaceous, five and one-
half centimeters long, and as broad below the middle, where it is some-
what enlarged; five palmately nerved from the base, the lateral veins
diverging about equally in an augle of Z(P from each other, so that the
inner one ascends to the two thirds of the leaf, the second to below tbe
middle, and the basilar veiulets are in right angle to the midrib. The
primary veins branch on tbe outside, anastomose with nervilles, and
tbe exteiior ones curve along and follow the borders; the secondary
veins are at an open angle of divergence of GO^, separated by strong
uervilles at right angle to the middle nerve. The areolation is obsolete.
Habitat. — South of Fort Barker, Kansas, C/w. Sternberg,
Menispebmites ovalis, sp. nov. PI. Y, fig. 4.
Leaf narroicly oval oblong, obtuse rounded at the base; fivepalmately^
nerved ; lateral veins on an acute angle of divergence, the inner ones as-
cending to near the top, branching outside ; brandies numerous, parallel,
curving along the border in multiple festoons.
This fine leaf, preserved nearly entire, is subcoriaceous, seven and one-
half centimeters long, three and one-half centimeters broad, nearly exactly
oval-oblong, perfectly entire and rounded to the base. The palmately
five nervation is less definite than in the former leaf; the two internal
lateral veins are as strong as the middle nerve, curve gradually in the
same direction as the borders, and, near the top, join the branches of the
midrib, with which they anastomose in curves ; tbe outside lateral veius
are thinner and shorter ; they ascend nearly parallel to the borders, but
disapi)ear in the middle of the leaf in anastomosing with branches of tbe
inside primary veins. In comparing this nervation with that of the
358 GEOLOGICAL SURVEY OF THE TERRITORIES.
former species and also with that of the other leaves referred to this
division, its identical type will be easily recognized and its relerenoe to
this genus found appropriate.
Under the name of Daphnogene Kaniiy Professor Heer has published in
the Arctic Flora, 1, p. 112, PI. XIY, from the Miocene of Greenland, leaves
which by form and nervation are closely related to this Cretaceoas
species. In the flora of Gelinden by Saporta and Marion, fragments of
leaves of the same character are referred to the Menispcrmacece and
described nnder the generic name of Cocculus. The Cietaceous form
here described is intermediate between the Tertiary species and those
described here from the Dakota group.
Habitat. — Near Clay Center, Kans,, H. d Towner.
Menispermites cyclophyllus, sp. nov. PL VI, fig. 4.
Leaf suhcoriaceou8^ entire^ nearly rotmdj peltate fnyin near the middle^
deeply concave^ palmately five nerved; inner lateral veins curving inside
toward the point; the outer ones open nearly at right angle to the middle
nerve^ all dividing by open straight branches; basilar veinlets three^ passing
down and curving along tJie borders.
The first of these leaves figured here is not quite as well preserved as
a larger specimen obtained lately. The essential characters are« how-
ever, distinctly marked. Excepting the modification in relation to the
form of these leaves, and the point of attachment of the petiole, the
nervation is of the same type as in the former species As observed
upon the larger specimens, three or four veinlets pass downward from
the lower part of the point of attachment of the i>etiole, curving on
ea<ch side and following the borders in festoons, like marginal veinlets..
The tertiary nervation, which is distinct and as marked upon the upper
part of the figure, is exactly of the same type as in the former species,
the veinlets nearly at right angle or slightly oblique to the secondary
veins, forming a double series of outside curves like superposed arches,
the last row following the borders in festoons. The leaf figured as
marked above is concave to the round point of attachment of the peti-
ole, which passes down into the stone, leaving an opening like the pipe
of a funnel. In the larger leaf, which is ten centimeters broad and
eight long, the depression is not as marked and the surface is nearly
flat. On this specimen the primary veins and their branches pass up to
near the borders before dividing, and thus have a nervation remarkubly
similar to that of Menispermites Salinensis, as represented in Cret. Flora,
PI. XX, fig. 1.
Habitat. — Kansas, near Fort Barker, the first leaf, Chs, Sternberg,
Near Clay Center, the largest specimen, H, C. Towner.
MALYACE^.
Sterculia lineariloba, sp. nova.
Leaf truncate to a short thick petiole^ largcy divided to near ihe base in
five linear-entire^ nan'oWy obtusely-pointed lobes about equally diverginffy
from acute sinuses,
I know this fine leaf only from a sketch communicated by the owner
of the specimen. It is seventeen centimeters broad between the points I
of the lower lobes, which are in right angle to the middle one, eleven
centimeters long from the top of the petiole to the point of the middle
lobe, which is eleven centimeters long from the sinuses; flve-palroately
nerved from the base ; lobes nearly linear, narrowed into a short poin^
J
LMQUEBEux.] ENUMERATION OF CRETACEOUS PLANTS. 359
entire; nerves very thick, secondary veitia and areolation obsolete.
This leaf may be referable to Aralia^ bot it appears more evidently
related to Sterculia by its truncate base and its narrow linear lobes^
Habitat.— Near Clay Center, Jff. C. Towner.
TILIACE^.
OBBVIOP8IS Haydenh, Lesqx., Cret. Flora, p. 97, PI. Ill, figs. 2, 4; PL
XXIV, fig. 3.
Leaves large^ broadly ovate^ tapering up to a point, more or less abruptly
narrowed to the base; borders equally denticulate from below the middle;
nervation irregularly pinnate or abnormally five-palmate, cra^edodrome.
In regard to these leaves, whose attribution is not positively known,
Count Saporta remarks that by their facies they resemble leaves of
Corylopsis, a generic division of the HamameKdce^ especially represented
iu the Japan flora ; the attribution would be therefore a natural one.
These leaves, however, appear equally related by some of their charac-
ters and by their facies to the Tiliacece.
AOERACE^.
NifiGtJNDOiDES ACUTiFOLius, Lesqx., Cret Flora, p. 97, PI. XXI, fig. 5.
Leaves irregularly cut; leaflets thin, lanceolate-pointed or enlarged lobate,
with acuminate lobes, pinnately veined ; veins camptodrome.
No other fragments referable to this have been discovered. The true
character of the leaves represented by the fragments is uncertain.
CELASTBACE^.
Celasteophyllum ensipolium, Lesqx., Cret. Flora, p. 108, PL XXI,
figs. 2, 3.
Leaves very thick and coria^ieous, linear, abruptly contracted to the base
by a round curve, broadly deltoid-pointed, borders undulately crenaie or
merely undulate; nervation pinnate^ secondary veins close, parallel camp-
todrome, diverging in acute angle from the thick middle nerve.
aquifoliaoeje.
Ilex stranoulata, sp. nov. PI. VIII, fig. 3.
Leaf coriaceous, narrow, panduriform or strangled in the middle to a
small angular lobe; rounded and narrowed to the petiole, entire toward the
base;, upper part enlarged oval f point broken J, oorders irregularly, dis-
tantly, obtusely dentate, secondary veins close, nearly at right angle to the
middle nerve, irregularly camptodrome.
This leaf is about five and one-half centimeters long without the
petiole, which measures one and one-half centimeters; its broadest part
above the petiole, as below the point, is not more than twelve milli-
meters, and in the middle, where it is contracted, two millimeters only.
Its texture is thick; the surface rugose; the secondary veins generally
very open, though variable in their direction ; curve near, and along
the borders, forming a more or less distinct narrow margin. The
areolation distinct only at one place, where tbe epidermis is destroyed,
is in small angular generally square areoIsB. The deformed shape of
this leaf, its border, its thick texture, and nervation, indicate its relation
to this genus.
360 GEOIiOOICAL SURVEY OF THE TERRITORIES.
Habitat. — Same as Dryophpllum salioifoliumy in connection with coal
strata of Southwest Colorado, at a higher stage of the Cretaceoofi^
H, Holmes,
These two last-named species have no relation known as jet with
any of the Dakota group, and none also with species of the Lower
Lignitic or Eocene. Their affinity appears to be with a group of plants
known from specimens of the upper stage of the Cretaceous of New
Jersey. Indeed, the two horizons where fossil leaves have been foand
in this State, i*epresent, by the lithological composition of the strata,
their relative distance, and the characters of their fossil leaves, a striking
affinity with what is seen in the stratification, the composition, and the
plants of the formation referred above and reported by Mr. Holmea
The Lower Cretaceous of New Jersey is composed, as far as I could
judge from the specimens which lezamiued, of sandy, white, or reddisk
coarse shale, wherein the plants are imbedded in profusion, but in a
poor state of preservation. These represent many species identical
with those of the Dakota group, or at least evidently related forms.
Both Magnolia Capellini and especially Magnolia alteman^j are among
them. The upper group, on the contrary, has scarcely any identical
species with those of the lower, though the intervening space is not
more than one hundred feet; its types appear generally different, and
as the vegetable remains are found in a soft clay, the leaves are far
better preserved. Among the species of this Upper Cretaceous group,
one is apparently closely related to the Dryophyllum described from
Mr. Holmes's specimens.*
FRANGULACEiE.
Paliurus membranacbus, Lesqx., Cret. Flora, p. 108, PI. XX, fig. 6.
Leaf sniallj memhrana^ieoiis^ ovalj obtuse^ entire^ palmately three-nerred
from the base ; lateral veins thin ; nervilles distinct, in right angle to the
veins and joining them.
Bhamnus tenax, Lesqx., Cret. Flora, p. 109, PI. XXI, fig. 4.
Leaf entire, lanceolate-pointed or acuminxitej narrowed by a curve. to a
short petiole ; lateral veins close^ numerous j thin, parallelj c-amptodrame,
TEREBIMTHAO&iB.
JuGLANs! Debeyana, Hcer, Cret Flora, p. 110, PI. XXIII, figs. 1-5.
Leaves coriaceous, entire, broadly ovate, obtuse, or unth a short obtuse
point, rounded-subcordate at the base, or narrowed by a curve and slightly
decurring to the petiole ; middU nerve thick ; secondary veins numerous,
open, camptodrome.
It has been remarked, in the introduction, that these leaves may be
referable to Rhtis. Count Saporta remarks that if there is among these
leaves a proportionate number of them with unequilateral base, Iikefig8«
4 and 5, they may indeed represent a Juglans or a Juglandites.
* Theae specimens were received after my return from New Jersey, where, by the
kindness of Dr. G. H. Cook, the director of the f^eological survey of that State, I had
the privilege of examining the numerous materials of the State coUectioD. I have not
had yet opportunity of comparing the specimens of Colorado with those of Kev
Jersey, and speak therefore from memory.
LMQUKBEUx.] ENUMERATION OP CBBTACEOUS PLANTS, 361
Phyulites EHOiFOLius, Lesqx., Cret. Fior., p. Ill, PI. XXII, figs
5 aud 6.
Leaves coriaceous^ lanceolate penninervey irregularly obtusely dentate;
middle nerve thick; secondary veins parallel^ comptodrome^ deeply marked.
PetjnusI ceetaceus, Lesqx., Cret. Flora, p. Ill, PL XXUI, figs.
8 and 9 5— PI. IV, fig. 9.
Drupe ovate, obtusely pointed^ grooved on one side to the middle^ notolied
at the enlarged obtuse base.
Nothing new has been elicited in regard to the relation of this fruit,
though another specimen has been found apparently representing the
same species. As seen in fig. 9 of PL IV, it is exactly of the same size
and form as the one in PL XXIII, fig. 8, of the Oret. Flora. It is
upon the surface of a large flat fragment of sandstone, where it is im-
bedded to the middle of its thickness, the part figured being very dis-
tinct. From the remnants of a thin coat of matter sioiilar to a shelly
envelope, it seems to have been surrounded by a coriaceous pericarp.
The same specimen represent a leaf of Aralia towneri.
Habitat.— South of Clay Center, Kansas, H. C. Towner.
INCEBTJB SBDIS.
ASPIDIOPHYLLUM, Lesqx.
Leaves large, triangular in outline, palmately trilobed, truncate and
auricled at base ; nervation coarse, prirnary nerves three from above the
peltate top of the petiole; secondary veins close, parallel, camptodrome or
craspedodrome.
The essential diflerence separating the leaves of this new division
from those of Sassafras {Araliopsis) is the broadly peltate and auricled
base. As seen from Plate II, fig. 1, the lateral veins are very open,
nearly at a right angle with the middle one, and therefore the lobes
have the same direction, and the leaf has nearly the appearance of a
cross; these short broad lobes, either obtusely dentate by the extension
of the point of the secondary veins entering them, or entire whenever
these veins curve along them, are remarkably similar to those of 8.
Harkerianum. The secondary nervation, however, is of a somewhat
different character, the veins being more curved in passing up to the
borders, and also at a more obtuse angle of divergence. The rounded,
more or less elongated auricle is nerved by the downward continuity of
the secondary veins, or, as seen in fig. 2, by two pairs of secondary
veins in right angle to the middle nerve, and two pairs of marginal
veinlets from the top of the petiole. This disposition has analogy to
the basilar nervation of Credneria leaves; with the diflference, however,
that in Credneria all the lower secondary veins are at a right angle to
the midrib. The same kind of afiSnity is still more marked with species
of Profx>phyllum, as for example P. multinerve, Cret. Flor., PL XVIII,
fig. 1, whose leaves, however, are not lobed, and whose upper nerva-
tion is of an entirely different type. We have therefore still in these
leaves a union of different characters separately and distinctly recog-
nized in other groups of this remarkable flora.
ASPIDIOPHYLLUM TBILOBATUM, Sp. UOV. PL II, tigS. 1, 2.
Leaves large, coriaceous, triangular or rhomboidal in outline, more or
less deeply trilobate, broadly cuneate to tJie base, enlarged into an half -round
auricle, threenerv&Afrom above the peltate base of the thick middle nerve*
These leaves vary in size from ten to twenty-four centimeters long and
362 GEOLOGICAL SURVEY OP THE TERRTTOBIES.
from twelve to thirty ceutimeters broad between the points of the lateral
lobes ; these are tnrned upward in the normal form, the angle of diver-
gence of the lateral veins being 4(P to 50^, with a very deep coarse
nervation. The borders of the lobes are more generally dentate, and the
veins, therefore, mostly craspedodrome.
I was disposed to consider as a separate species the leaf represented,
fig. 1, greatly differing by its diminutive size, the direction of the lobes,
and the still broader nervation. These leaves, of which we have two
specimens, have the surface rnncinate, or appearing as if they were not
fully unfolded ; they represent probably a peculiar form or variety of the
same species, for, except this difference, the characters are the same.
Habitat. — South of Fort Barker, Kansas, Chs. Sternberg.
Pbotophyllum Stebmbergii, Lesqx., Cret. Flora, p. 101, PI. XVI;
PL XVJII, fig. 2.
Leaves large^ coriaceops^ peltate entire^ rounded or cordate at ba^te^ grad-
ually narrowed up into a slightly obtuse point ; basilar reins one or tus) pairs,
Pbotophyllum Lboonteanum, Lesqx., Cret Flora, p. 103, Pi. XVII,
fig. 4 J PI. XVI, fig. 1.
Leaves coriaceous^ rounds mare enlarged in the middle^ entire; middle
nerve thicJcj lowest secondary veins much divided^ basilar veins in right
angle to the middle nerve proportionally thicJc.
Pbotophyllum ! Kebbasgense, Lesqx., Cret. Flora, p. 103, PL XXVII,
fig. 3.
Leaf smalls subcoriaceous^ oval-oblong^ abruptly narrowed to the petiole ;
borders entire^ middle nerve thin^ secondary veins eloscy parallel^ all under
the same angle of divergence.
This leaf is by its character referable to the generic division of the
Hamamelit^j and clearly related to the leaf of our PL VII, fig. i.
Pbotophyllum QUADEATUM, Lesqx., Cret. Flora, p. 104, PL XIX, fig. 1.
Leaves thickish^ subcoriaceous^ round-square in outline ; truncate at the
base and subpeltate^ deeply undulate^ obtuse; nervation thick^ secondary
veins straight to the borders.
Peotophyllxtm MINUS, Lesqx., Cret. Flora, p. 104, PL XIX, fig. 2 ;
PL XXVIl, fig. 1 ;— PL V, hg. «.
Leaves small, coriaceous j broadly ovate, truncate orsubcordate at the ba^ ;
entire or slightly undulate, subpeltate.
These different forms of Protophyllum are clearly defined and preserve
their characters in the numerous specimens which I have had for exam-
ination. PL IV, fig. 6, shows a very small leaf of this species, repre-
senting in miniature the large forms described in the Cret Flora.
Pbotophyllum multinebve, Lesqx., Cret. Flora, p. 105, PL XVIII,
fig. 1.
Leaves of medium size, coriaceous, oval-oblong, round-truncate at the base,
peltate, middle nerve thick, secondary veins close, numerous, in an open
angle of divergeme, the lower ones in right angle and deflecting downwardj
borders entire or undulate.
Pbotophyllum buqosum, Lesqx., Cret. Flora, p. 105, PL XVII, figs. 1
and 2 ; PL XIX, fig. 3.
Leaves deltoid-ovate, rounded and subpeltate at the base, borders eiUire;
nervation coarse^ surface rugose^ secondary veins irregular in distance a»d
direction.
LESQURREux] ENUMEBATION OP CRETACEOUS PLANTS. 363
Pbotophyllxjm Hatdbnii, Lesqx., Cret Flora, p. 106, PL XVII, fig. 3.
Leaves small^ coriaceouSj smoothj obUmg-ovate^ pointed^ deeply irregularly
nndulate-lobed, abruptly rounded to the ha^e^ subpalmately three-nerved;
secondary veins parallel, straight to the borders^ basilar veins two or three
pairs at right angles to the middle nerve.
The basilar nervation of this species, as also of the following, is of the
Credneria type.
Peotophyllum gbednebioides, 8p. nova. PL III, fig. 1; PL VIII,
fig. 4.
Leaves small, nearly round, truncate at tlie hase^ long pctioled ; borders
entire, undulate ; nervation obscurely trifid ; secondary veins on various
angles of divergence.
These leaves, of which we have many specimens, vary in size from six
to eight centimeters, and are as broad as long ; they are more or less
deeply uudalate, bat the borders are entire, though all the veins and
their divisions pass to the borders; the petiole is comparatively long
and slender and the secondary veins more or less open, according to
their position, being at a right angle to the middle nerve near the base
and at an acute angle of divergence near the top. As in the former
species, the leaves are obscurely tripalmately-nerved, the lower lateral
primary veins above the borders being underlaid as in Credneria by two
pairs of thinner veins in right angle. In this case, however, as these
lower veins branch, and have the same direction as those above, they are
rather secondary veins, like the others, and the nervation should be
considered as pinnate.
Habitat.— Mostly found near Fort Barker, Kansas, Cits. Sternberg.
Pbotophyllum! Mudgei, Lesqx., Cret. Flora, p, 106, PL XVIII, fig. 3.
Leaf thicJ:, coriaceous, ovate-obtuse, enlarged and truncate at base, equally
denticulate ; middle nerve very thick ; secondary veins alternate^ mere or less
branching, craspedodrome.
The leaf, the only fragment of > which is figured, is of uncertain refer-
ence.
Anisophylltjm semi-alatum, Lesqx., Cret. Flora, p. 98, Pi. VI, figs.
1-5.
Leaves thicJc, coarsely veined, ovate or obovate in outline^ eitlier abruptly
narrowed J subtruncate and subcordate to tJie petiole, or rounded wedge form
to the base, irregularly lobate on one sidCy deeply undulate on the borders ;
nervation irregularly three to five palmate from above the base of the leaves ;
primary veins much divided.
Bbbmophyllum fimbbiatum, Lesqx., Cret. Flora, p. 107, PL VIII,
fig. 1.
Leaf peltate, Jcidney-shaped^ with an entire broadly truncate base ; bor-
ders dentate by equal hastate or auricled, and pointed teeth; nervation
seven palmate.
VEGETABLE ORGAinSMS OP UNCERTAItf AFFINITY. .
Phtllites BETULiEFOLixJS, Lesqx., Cret. Flora, p. 112, PL XXVIII,
figs. 4, 7.
Leaves smally mostly in fragments^ round-ovate^ truncate at the top, nar-
rowed to the base by a round curve; borders dentate; nervation pinnate^
irregular^ craspedodrome.
364 GEOLOGICAL SUBYET OF THE TERRITORIES.
Phyllitbs bhomboideus, Lesqx., Oret. Flora, p. 112, PL VI, fig. 8.
Leaf rhomboidal^ hrondly cuneate to the bdscj more obtusely narrowed and
undulate from the middle to an obtuse short point ; nervation five-palmate
from Hie base^ the two inner lateral veins curving up at a very acute angle
of divergence and aerodrome or nearly reaching the point of the leaf branching
outside, tJie external veins following the borders up to the middle of the leef^
where they anastomose with branches of the first pair.
Phyllites cotinus, Lesqjc
BuMELiA MARCOUANA, Hcer (Le«qx.)» Cret. Flora, p. 90, PI. XXVIII, fig. 2.
Leaf membranaceo^iSy broadly ovaly entire^ emarginatCy rounded downward
to a long slender petiole, penninerve.
From information received of Professor Heer, this leaf positively
differs from the one which he examined and which is figured in
Dana's Manual of Geology. Though the likeness of this leaf to those
of Bhus cotinus is marked, its relation is not definite.
Phyllites Vanon^, Heer,— Cret. Flora, p. 113, PI. XX, fig. 7 : PL
XXVIII, fig. 8.
Leaves small, ovate-lanceolate, pointed, cuneiform to the base; borders en-
tire, middle nerve thin, secondary veins jfew^ scattered^ camptodrome.
Phyllites itmbonatus, Lesqx., Cret. Flora, p. 113, PL XIX, fig. 4.
Leaf quadrate in outline, truncate at the base, deeply notched at the top by
the splitting of the thick middle nerve, irregularly broadly undulate on the
borders; secondary veins few, at irregular distances, nearly at right angle to
tlie middle nerve, camptodrome.
m
Phyllites amobphus, Lesqx., Cret. Flora, p. 113, PL XXI 1, figs. 3, 4.
Two fragments of coriaceous, obovate, entire leaves, narrowed to the base
(broken) ; middle nerve deep and narrow ; secondary veins either in right
angle to tlie middle nerve or curved downward, or passing up in an acute angle
of divergence, branching and anastomosing in varions abnormal icays.
Ptenosteobus nebbascensis, Lesqx., Cret. Flora, p. lli, PL XXIV,
fig. 1.
Cone oblong, cut in its length ; seeds oblong-oval, lenticular, obtuse at one
end, pointed at tfie otlier, winged, wings oval oblong, striated.
Caulinites spinosa, Lesqx., Cret. Flora, p. 115.
Stems or branches cylindrical, tcith rough surface marked by irregular,
close dots, or small cavities resembling the impressions of scale ; bearing long
spines at right angles.
Cabpolithes ?, Cret. Flora, p. 114, PL XXVI, fig. 5, PL XXX, fig. IL
Fruit t large, oval-pointed at both ends, costate, marked at the lo^cer end
by a small hollow surrounded by small semi-globular bolsters corresponding
with the end of the costas.
The bodies represented by the figures are doubtfully referred to some
vegetable organism.
It would, perhaps, seem advisable to close this review by a table of
comparison, exposing the relation of the species of the Dakota group
with those of the Cretaceous floras of other countries. A table of this
kind, however, would not offer any valuable information, and could be
of little interest, on account of the scantiness of the materials available
for comparison. The few points of afiSnity between our American Cre-
utaQURBEUx.] REVIEW OP CRETACEOUS FLORA. 365
taceous plants and those of Earopehave beeu remarked in the Cretaceoas
Flora, and, since its publication, no other work has appeared on the same
sabject but the third volume ot the Arctic Flora, where, as remarked be-
fore, Professor Heer describes the species of fossil plants from two stages
of the Cretaceous of Greenland ; a lower one, that of Gome ; an upper one,
that of Atane, and an intermediate small group from Spitzberg. With
the species of the first division, the Dakota group flora has Gleichenia
nordemkioldi, identical and none related ; with those of the second, it
has two Conifers — Sequoia fastigiata and Finns Quenstedii. This last has
been described also b.v the author, from Spitzberg, and formerly from
Moletin. In the monocotyledonous. our Phragmites cretaceous seems
identical with Arundo greenlandica, Beer, of the same upper stage, and
in the dicotyledonous, Myrica cretacea^ Lesqx., is comparable to M.
zenleri^ Heer, which is represented by a fragment only. There is still
an evident relation of the leaves described by Heer as Chondrophyllum
arbiculatum and (7. nordenskioldi with those of Hedera ovalis^ of the
Dakota group. We have also Andromeda Partatorii^ Magnolia Capellinij
and AL altemans present in both floras. These three species are appa-
rently extensively distributed in the Cretaceous.
Without taking into account the more or less acceptable modifications
of generic and specific forms proposed in this review, we have here an
addition to the North American Cretaceous flora of twenty-four species,
mostly clearly defined from very tine specimens. This contribution, the
result of the discoveries made during one year only, by two zealous
young naturalists who have explored merely an area of small extent in
the counties where they live, shows what abundant materials are still
left in the strata of the Dakota group to reward future researches. It
exposes, also, with more evidence the riches and the diversity of the
vegetation of the Cretaceous [>eriod, manifested as it is by the distribu-
tion of the dicotyledonous leaves in the three great divisions of this
class of plants; by the numerous, clearly -limited, generic groups which
they represent, as well as by the multiplicity of specific forms referable
to some of the genera. The species of Menispermites and of ProtophyU
lum^ for example, are as distinctly separated by the characters of their
leaves, though prest^rving the unity of their generic type, as we see
them at the present time under analogous climatic circumstances.
These facts tend to confirm the general conclusions briefly exposed in
the Cretaceous Flora concerning the origin and the distribution of the
dicotyledonous species, a question to which the history of our present
North American flora is interested in the highest degree.
EXPLANATION OF PLATE L
Fig. 1. Akaua tripartita, sp. nov., page 348.
Fig 2, 2*, A R ALIA Saportanra, sp. nav.y page 350.
HidteL
J •• f /c %
•- t
'y
/
/
EXPLANATION OF PLATE IL
Figs. 1, 2. A8PIDIOPHYLLUM TRiLOBATUM, «p. 110V., page 361.
Fig. 3. Ampblophyllum attenuatcm, sp. nor., page 354.
Fig. 4. Phtixogladus subintegrifolius, Leaqx., page 337.
Figs. 5, 5^. Gleichbnla nordenskiOldi, Hear,, page 334.
FlntelL
v««*
Library.
'*t ,.
« •>• %
EXPLANATION OF PLATE IH.
Fig. 1. PHOTOPHYLLUM CKEDNRRIOIDES, Sp, ttOt*., page 963.
Figs. *2, 8, 8*. Sequoia fastigiata, Sfemb., page 335.
Fig. 3. Hedrka platanoidea, sp. nov.^ page 35L
Fig. 4. MvRiCA CRETAOEA, sp. ftor., page 339.
Fig. 5. Androbaeda akfinis, sp. nop., page 348.
Pigs. 6, 6», 7, ?•. PiNUS QUENSTEDTi, Heer,^ page 336.
J
\
f/
Library.
/
<-, "r (« -p T-'
EXPLANATION OF PLATE IV.
Fig. 1. AJtAUA ToWNKBi, sp, nov,f page 349.
Figs. 2-4. Abalia concrkta, sp, nov.^ page 349.
Figs. 5-7. Skquoia condita, sp. nov.^ page 335.
Fig. 8. iNOLEPis f y tfpectes., page 337.
Fig. 9. PRUNUS r CRKTACEA, LeBqx., page 361.
Pfclte]^
EXPLANATION OP PLATE V.
Figs. 1 and 2. Laurus prote^folia, sp, nov., page 342.
Fig. 3. Mkmispermitrs populifouus. ep. nov., page 357.
Fig. 4. Mekispermites ovALiSy «p. HOP., page 357.
Fig. 5. Ficns DI8TORTA, «p. nor., page 342.
Fig. 6. PROTOPHYLLUM MINUS, Lesqx., page 362.
Fig. 7. Ficus LAUROPHTLLUH, Xm^k., page 342.
'HsV.
"*
»- »
' */
J
I* •
I
■
EXPLANATION OF PLATE VI.
Fig. 1. Drtophyllum (qubrcus) latifolium, irp. not., page 340.
Fig. 2. LoMATiA 8APORTANBA. Lesqx. An enlarged leaflet, page 346.
Fig. 3. CissiTKS HEERii, sp. ncw., page 353.
Fig. 4. Menispermites cyclophyllus, flp. nov,f page 358.
;_^.g -.•.■'. -,'.%
»
'^;.
' i^ vary,
f »«
/
,*
EXPLANATION OF PLATE VIL
Figs. 1 and 2. Cissites Harkkrianus, Z>«9Jr.,page 352.
Fig. 3. Mbnirpermitks obtusiuoba, Lesqx., page 356.
Fig. 4. Habiamelites Kansasbana, Lesqx., page 355.
Fig. 5. Hedera Schimpeki, sp, nov., page 351.
J
Library.
Of , , ,f, J, »
EXPLANATION OF PLATE VIII.
Fig 1. CissiTES ACUMiNATUS, «p. HOT., page 353.
Fig. 2. DRYOPHTLI.UM (QuKRCUs) 8ALICIF0LIUM, «p. nof ., page 340.
Fig. 3. Ilex straxoulata, sp. nov., page 359.
Fig. 4. Protophyllum ckkdnbrioidbs, sp. nov., page 363.
Fig. 5. Platanus Hbrrii, Lesqx,, page 341.
Hite\in
!>*«»/;:
Library.
0(
'« f r
EXPLANATION OF PLATE VIII.
Fig 1. C188ITES ACUMINATU8, «p. nor., page 353.
Fig. 2. Dryophtllum (Qukrgus) salicifolium, 9p, nor., page 340.
Fig. 3. Ilex stranoui^ta, tp. nor., page 359.
Fig. 4. Protophyllum crkdnbrioidbs, «p. nor., page 363.
Fig. 5. Platanus Herrii, Le9^, page 341.
HxteAin
fre«A/^
Library, j
^f i m if"rr>
REPORT OF W. H. JACKSON.
m
^ t
t ^ ^\
r : '
!'■ . /
y
ANCIENT RUINS IN SOUTHWESTERN COLORADO.
Br W. H. Jackson.
In the extreme sonthwestem corner of Colorado Territory, west of the
one hundred and eighth degree of longitude, are groaps of old rained
houses and towns, displaying a civilization and intelligence far beyond
that of any of the present inhabitants of this or adjacent Territory.
We will endeavor, in the few pages following, to describe these with
as mnch minoteness and circnmspection as a very hasty trip enabled
as to observe; depending more upon the pictorial illustrations accom-
panying this article for clear exposition of the subject than npon any
choice of words.
Although ruins in considerable number and importance were said to
exist along the Bio Las Animas and Ban Juan, we did not think it l>est
to spare any of the little time at our disposal for their investigation.
Oar object being to find those in which the picturesque predominated
and were the least known, we directed our course to the westward, hav-
ing obtained reliable information of the existence of some which would
come up to our anticipations. The Kio Mancos, one of the western trib-
utaries of the San Juan, rises in two principal forks among the western
foot-hills of the Sierra La Plata, flows southwesterly through fertile and
beautiful valleys to a great table-land, known asi the ^^ Mesa Verde,"
and entering, flows directly south through it to the valley of the San
Jnan, and then turning west again joins that stream near the crossing
of the boundary-lines of the four Territories.
Commencing our observations in the park-like valley of the Mancos
between the mesa and the mountains, we find that the low benches which
border the stream upon either side bear faint vestiges of having, at some
&r-away time, been covered with dwellings, grouped in communities
apparently, but now so indistinct as to present to the eye little more
than unintelligible mounds. By a little careful investigation, however,
the foundations of great square blocks, of single buildings, and of circu-
lar inclosures, can be made out ; the latter generally with a depressed
center, showing an excavation for some purpose. The greater portion
of these mounds are now overgrown with artemisia, pifion-piue, and
cedar, concealing them almost entirely from casual observation. We
foond the surest indication of their proximity in the great quantity of
broken pottery, which covered the ground in their neighborhood, the
same curiously indented, painted, and glazed ware found throughout
New Mexico and Arizona. It was all broken into very small pieces,
none that we could find being larger than a silver dollar. We had no
opportunity to make any excavations about these old mounds ; but such
little scratching around as we c^uld do developed nothing new below
the surface, all the pottery which covers the ground having been broken
and scattered since the demolition of the homes of the makers. No-
where among these open-plains habitations could we discover any ves-
tiges of stone-work, either in building material or implements. It is
309
24 n
370 GEOLOGICAL SURVEY OP THE TEREITOEIES.
very evident that the houses were all of adobe, the mound-like charae-
ter of the remains jastifying that belief.
The ^^ Mesa Verde" extends north and south about twenty, and east
and west aboat forty miles. It is of a grayish-yellow Cretaceous sand-
' stone, with a very' nearly horizontal bedding, so that the escarpment is
about equal upon all sides, ranging from 600 to 1,000 feet in height.
The capping or upper strata are generally firmly and solidly bedded,
retaining a perpendicular face of aboat 200 feet, with a succession of
benches below, connected by the steep slopes of the talus. Side-canoos
penetrate the mesaj and ramify it in every direction, always presenting
a perpendicular face, so that it is only at very rare intervals that the
top can be reached ; bat, once up there, we find excellent grazing, aod
thick groves of cedar and pinon-pine. From the bottom of the canon
up, the slopes of the escarpment are thickly covered with groves of cedar
and piOon, gnarled and dwarfed, bat sucking ap a vigorous livelihood
from the cracks and crevices of the barren declivities. Below, the Cot-
tonwood and willow grow luxuriantly beside the streams, while dense
growths of a reed^' grass tower above our heads as we ride through it
Throughout its entire length, the canon preserves an average width of
about 200 yards, sometimes much wider and again narrower. Hie
stream, meandering from side to side, frequently interrupted by beaver-
dams, cuts a deep channel in the friable earth which characterizes all
the valley-lands of this region, while the banks upon either one side or
the other are perpendicular, so that it is an extremely troublesome mat-
ter to cross. Added to the difficulties of getting in and out of the
stream is a thick matted jungle of undergrowth, tall, reedy grass, wil-
lows, and thorny bushes, all interlaced and entwined by tough and wiiy
grape-vines bordering its banks upon either one side or the other. The
current is sluggish, and the water tinged with a milky translucency,
gathered from the soil.
Entering the canon at its upper end, we strike into the old Indian
trail whi3h comes over from the head of the Bio Dolores, and, xiassing
down this canon a short distance, turns off to the left and goes over to
the La Plata. About a hundred Indians had just passed over it with
their horses and goats, so that it was in most excellent traveling order,
although winding in and out, and over and among great blocks of sand-
stone and other d&ma from above ; the encroaching stream, too, fire-
queutly forcing the narrow pathway high up on the slopes of the pro-
jecting spurs, the treacherous character of the banks of the stream for-
bidding the crossing and recrossing usual in such cases. Grouped along
in clusters, and singly, were indications of former habitations, veiy
nearly obliterated, and consisting mostly, in the first four or five miles,
of the same mound-like forms noticed abpve, and accompanied always
by the scattered, broken pottery. Among them we found one building
of squared and carefully-laid sandstone : one face only exposed, of three
or four courses, above the mass of ^om, which covered everything.
This building lay within a few yards of the banks of the stream } was
apparently about 10 feet by 8, the usual size, as near as we could deter-
mine, of nearly all the separate rooms or houses in the lai^^ Uocks,
none larger, and many not more than 5 feet square. The stones ex-
posed are each about 7 by 12 inches square and 4 inches thick, those in
their original position retaining correct angles, but, when thrown down,
worn away, and rounded by attriticm to shapeless bowlders. Bewg so
exposed to the elements, the cementing material which bound the ma-
sonry together is entirely worn away upon the surface; but, upon poll-
ing away a few courses, it was found binding the rocks together quite
t
Library. .
*
4
Library.
tvest^
4.
rary.
Of ,
y
/
jACKsoK.] ANCIENT RUINS IN 8. W. COLORADO. 371
firmly. It was not, however, anything more than an adobe or clay-
cement.
A.S we progressed down the caiion, the same general characteristics
lield good; the great majority of the rains consisting of heaps of
dibrisy a central mass considerably higher and more massive than the
Horrounding lines of subdivided sqnares. Small buildings, not more
than 8 feet square, .were often found standing alone apparently ; no trace
of aD J other being detected in their immediate neighborhood.
^We now commenced to note another peculiar feature. Upon our right,
the long slopes of protruding strata and debris formed promontories,
extending out into the ca&on. Upon these, and not more than 50 feet
above the stream, we found frequent indications of their having been
occupied by some sort of works, the foundations of which in every case
were circular, with a deep depression in the center, and generally occur-
ring in pairs, two side by side, ranging from 10 to 20 feet in diameter.
Tbere was no masonry of any kind visible, but thickly strewn all about
any quantity of broken pottery. Above, were indications of habitations
in the faob of the clifT, but not marked enough to warrant further search.
At those places where the trail ran high up, near the more precipitous
portion of the bluff, we found remnants of stone walls, inclosing spaces
of from 5 to 12 feet in length, in the cave like crevices running along
the seams. They were pretty well demolished, the stones undressed
and imbedded in mud mortar. In many places, little niches or crevices iu
rock had been walled up into cupboard^ike inclosures of about the size
of a bushel-basket. We searched them eagerly, but they had all been
despoiled before us. Nothing of any greater importance was found up
to the time we made camp at nightfall. All that we had seen during
the day was of exceeding interest, but came far short of our expecta-
tions.
Our camp for the night was among the stunted pinons and cedars
immediately at the foot of the escarpment of the mesa; its steep slopes
and perpendicular faces rising nearly 1,000 feet above us. Quantities
of broken pottery were strewn across the trail, to the edge of the stream,
and as ruins of some sort generally followed, close attention was paid to
the surroundings ; but, with the exception of a small square inclosure
of rough slabs of stone, set in the earth endwise, and indicating, possi-
"^ly* A grave, nothing was found to reward our search. Just as the sun
was sinking behind the western walls of the canon, one of the party de*
scried far up the cliff what appeared to be a house, with a square wall,
and apertures indicating two stories, but so far up that only the very
sharpest eyes could define anything satisfactorily. We had no field-
glass with the party, and to this fact is probably due the reason we had
not seen others during the day in this same line ; for there is no doubt
that ruins exist throughout the entire length of the ca&on, far above
and oat of the way of ordinary observation. Cedar and pines also
grow thickly along the ledges upon which they are~1&uilt, hiding com-
pletely anything behind 'them. All that we did find were built of the
same materials as the cliffs themselves, with but few, and then only the
smallest apertures toward the cation ; the surface being dressed very
smooth, and showing no lines of masonry, it was only upon the very
closest inspection that the house could be separated from Uie cliff.
The discovery of this one, so &r above anythiug heretofore seen,
inspired us immediately with the ambition to scale the height and
explore it, although night was drawing on fast, and darkness would
probably overtake us among the precipices, with a chance of being de-
tained there all night All hands started up, but only two persevered
372 GEOLOGICAL SURVEY OF THE TERRITORIES.
to the end. The first 500 feet of ascent were over a long, steep slope of
dSbriSy overgrown with cedar : then came alternate perpendiculars and
slopes. Immediately below the house was a nearly perpendicular
ascent of 100 feet, that puzzled us for a while, and which we were only
able to surmount by finding cracks and crevices into which fingers and
toes could be inserted. From the little ledges occasionally foand, and
by stepping upon each other's shoulders, and grasping tnfr« of ynoco,
one would draw himself up to another shelf, and then, by letting down
a stick of cedar, or a hand, would assist the other. Soon we reached a
slope, smooth and steep, in which there had been cut a series of steps,
now weathered away into a series of undulating hummocks, by which
it was easy to ascend, and without them, almost an impossibility. An-
other short, steep slope, and we were under the ledge upon which was
our house, (Fig. 12, Plate III.) It was getting quite dark, so we delayed
no longer than to assure ourselves that it was all we hoped for, and to
prospect a way up when we should return the next morning with the
photographic outfit.
Bright and early, as soon as breakfast was dispatched, we commenced
the ascent. Mexico, our little pack-mule, with the apparatus npon hef
back, by sharp tacks and lively scrambling over the rocks, was able
to reach the foot of the precipice of which I have spoken above. Op
this we hauled the boxes containing the camera and chemicals by the
long ropes taken from the pack-saddle. One man was shoved np ahead,
over the worst place, with the rope, and tying it to a tree, the others
easily ascended.
The bouse stood upon a narrow ledge, which formed the floor, and
was overhung by the rocks of the clifi'. The depth of this ledge was
about 10 by 20 in length, and the vertical space between ledge and
overhanging rock some fifteen feet. The house occupied the left-hand
half as we face it ; the rest being reserved as a sort of esplanade, a small
portion of the wall remaining which cut it off from the narrow ledge
running beyond. The edges of the ledge upon which the house stood
were rounded off, so that its outside wall had to be built npon an inclioe
of about forty-five degrees ; the esplanade, too, had been* extended by
three abutments, built out flush with the walls of the house, npoo the
steeply-inclined slope, and giving support probably to a balustrade.
The house itself, perched up in its little crevice like a swallow's nest,
consisted of two stories, with a total height of about 12 feet, leaving a
space of two or three feet between the top of the walls and the over-
hanging rock. We could not determine satisfactorily whether any other
roof had ever existed or whether the walls ran up higher and joined the
rock, but we incline to the first supposition. The ground-plan showed a
front room about 6 by 9 feet in dimensions, and back of it two smaller
ones, the face of the rock forming their back walls. These were each
about 5 by 7 feet square. The left hand of the two back rooms projected
beyond the front room in an L. The cedar beams, which had divided the
house into two floora, were gone, with the exception of a few splintered
pieces and ends remaining in the wall, just enough to show what they
were made of. We had some little doubt ^is to whether the back rooms
were divided in the same way, nothing remaining to prove the tact,
excepting holes in the walls, at the same height as the beams in the
other i)ortion. In the lower front room are two apertures, one serving
as a door, and opening out upon the esplanade, about 20 by 30 inches
in size, the lower sill 24 inches from the floor ; and the other a small
outlook, about 12 inches square, up near the ceiling, and looking over
the caiion beneath. In the upper story, a window corresponding in
()!'!« * T-
JACMON.I ANCIENT RUINS IN 8. W. COLORADO. 373
size, shape, and position to tbe door below, commaDds an extended
view down the canon. The upper lintel of this window was of small,
straight sticks of cedar, of about the size of one's finger, laid close
together, the small stones of the masonry resting apon them. Directly
opposite this window is a similar one, opening into a large reservoir, or
cistern, the upper walls of which come nearly to the top of the window.
This is semicircular, inclosing the angle formed by the side wall of the
house against the rock, with an approximate capacity of about two and
a half hogsheads. From the window, and extending down to the bot-
tom of the reservoir, are a series of cedar pegs, alN)ut a foot apart,
eDabling the occupants to easily reach the bottom. The entire con-
struction of this little human eyrie displays wonderful perseverance,
ingenuity, and some taste. Perpendiculars were well regarded, and
the angles cai-efully squared. The stones of the outer rooms or front
were all squared and smoothly faced, but were not laid in regular
courses, as they are not uniform in size, ranging from 15 inches in
length and 8 in thickness down to very small ones. About the corners
and the windows, considerable care and judgment were evident in the
overlapping of the joints, so that all was held firmly together. The
only sign of weakness is in the bulging outward of the front wall, pro-
duced by the giving way or removal of the floor-beams. The back
portion is built of rough stone, firmly cemented together. The mortar
is compact and hard, a grayish-white, resembling lime, but cracking all
over. All the interstices between the larger stones were carefully
chinked in with small chips of the same material. The partitions were
of the same character as the smooth wall outside, both presenting some-
what the appearance of having been rubbed down smooth after they
were laid. The apertures, from one room to another, are small, corre-
sponding in size and position to those outside. Most peculiar, however,
is the dressing of the walls of the upper and lower front rooms, both
being plastered with a thin layer of firm adobe cement of about au
eighth of an inch in thickness, and colored a deep maroonred, with a
dingy white band 8 inches in breadth, running around floor, sides, and
ceiling. In some places it has peeled away, exposing a smoothly-dressed
snrface, of rock. No signs of ornamentation, other than the band al-
luded to, were visible. The floor, which was covered to a depth of 2 or
3 inches with dust, dirt, and the excrement of small animals, had been
evened up with a cement resembling that in the walls. The back rooms
were half-filled with rocky debris from roof and cliff.
While busied with my negatives, the others had prospected the ledge
in opposite directions, coming upon ample evidence of its having been
quite thickly ]>eopled. Ruins of half a dozen lesser houses were found
near by, but all in such exposed situations as to be quite dilapidated.
Some had been crushed by the overhanging wall falling upon them, and
others had lost their foot-hold and tumbled down the precipice. One
little house in particular, at the extremity of this ledge, about fifty rods
below the one described above, was especially unique in the daring of
its site, filling the mind with amazement at the temerity of the builders
and the extremity to which they must have been pushed. Careful
views of this having been secured so as to show as well as possible its
almost complete inaccessibility, we felt impelled to hurry on to new
developments. Apparatus was carefully lowered to the patiently-wait-
ing mule, and adjusted to the pack-saddle, then, mounting our own
animals, we pushed on down the canon, which now opened out into
quite a valley, side canons opening in from either hand, adding much
to the space. Every quarter-mile, at the most, we came upon evidences
374 GEOLOGICAL SUBTET OF THE TERBITOEIES.
of former habitations, similar to those already described; toe greater
majority occarring in the level bottoms and on the low spars of the
escarpment.
Two or three miles below the hoase in Fig. 12, we discovered a wall
standing in the thick brash apon the opposite side of the river. God-
siderable difficalty was experienced in crossing; in some places haviog
to cat oar way throagh the entangling vines witb oar belt-knives, and
then, when the bed of the stream was reached, bad to follow it aome
distance before an opportanity occnrred to emerge.
The walls before as were a portion of an old tower, (see Fig. 1, Plate ,)
in the midst of a groifp of more dimly marked rains or fonndations,
extending some distance in each direction from it. As seen in the
figure referred to, the tower consists of two lines of walls, the space
between them divided into apartments, with a single circnlar room in
the center. The oatside diameter of all is 25 feet, that of the inner
circle 12* feet, and as the walls were respectively 18 and 12 inches in
thickness, left a space of 4 feet for the small rooms. This oater circle
was evidently divided into six eqaal apartments, bat only the divisioDB
marked in the diagram conld be distingaished. In the places where
they shoald have occurred, the walls are so broken down and covered
with dSbris as to render all details indistingnishable. Where the waUs
are standing, they show small window-like doors opening into the inner
circle. The highest portion of the inner wall is now not more than 8
feet, and of the enter aboat 15. From the amount of dibriSj it coald
not have been mnch higher — not more than 20 feet at the most The
space between the walls is filled with dSbris^ while oatside there is very
little, except where the wall is totally rained.
The stones of which this tower was constrncted are irregular in size
and shape, but with the outer face dressed to a uniform surface, and of
the same average size as those already described. The mortar and
^'chinking" bad been worn out entirely ^om the more exposed portions,
giving the wall the appearance of having been dry -laid; but upon pall-
ing away some of the stones to a little depth, they were foand to have
been well cemented.
Passing on down the caiion, not stopping now to notice the more ordi-
nary forms of ruins, we passed the mouths of numerous side-canons,
down which come great freshets during the rainy season, gouging oat
deep arroyos, and strewing the surface with the collected deMs of pinon
and cedar, sage-brnsh and cacti. About the mouth of Goal Gafion, par-
ticularly, the whole surface of the " wash " was covered with lumps of
fine-looking bituminous (^oal, as though a thousand coal-carts had trav-
eled that way with their tail-boards out.
We camped at sunset at what our guide called the Rattlesnake Bend,
within a half dozen miles of the outlet of the caiion. We had not dis-
covered any more of the high cliff-bouses during the day ; bat there is
no doubt that, if we had had a good field-glass with us, many more might
have been found along the crevices near the summit of the escarpment
To have verified our suppositions by a personal inspecftion would have
involved a great deal of labor, and more time than we could have spared
from our very scanty store. In the vicinity of our camp, the canon
changed much in appearance; instead of the long slope of talus capped
* These dimeDsioiis were estimated from the photograph after leaving the locality,
not having the time or appliances for accurate measarement while there. The stiM
rain has since been examined by Mr. Holmes and accurately measured, with the foilow-
in«; results: Diameter over all 43 feet; of the inner circle, 25 feet. Mr. Holmes ako
makes out ten apartments instead of six. Bullotiu No. 1, vol. 2, p. 11.
Library.
jACKfiOK.1 ANCIENT RUINS IN S. W. COLORADO. 375
l>y a perpendicalar ledge, we have here a perpeDdicular ledge first, of
200 or 300 feet, and then a long receding bench, back to the higher mesa
l>e.yond.
Close to oar camp was one of the little towers that occar quite fre-
quently, about 10 feet in diameter, and now some 8 feet in height, with
the inside half-filled with the debris from the walls. Half a mile below,
ID the vertical face of rock, and at a height of from 50 to 100 feet from
tbe trail, were a number of little nest-like habitations. Fig. 5, Plate I,
illustrates one of them, and their general character. Communication
^ith the outside world was from above to a small window-like door, not
showing in the sketch. Two small apertures furnish a lookout over the
valley. The walls are as firm and solid as the rocks upon which they
are built. The stones are more regular in size than any noticed here-
tofore, but smaller. The chinking-in of small chips of stone is notice-
ably neat and perfect on the inside. This is not a commodious dwelling ;
15 feet would span its length, and 6 its height, while in depth it is not
more than 5 feet. Near by, upon a low ledge, and readibly accessible
from below, is a string of five or six houses, evidently communicating,
mere kennels compared with some others, made by walling up the deep
cave-like crevices in the sandstone. The same hands built them that
lived in the better houses; the masonry being very similar, especially
the inside chinking, which was perfect, and gave the walls a very neat
appearance. Fig. 8 of Plate II is an example of the tenacity of the mor-
tar; the view being of one of the line of little houses just spoken of.
In this case, a portion of the ledge upon which the house stands has
become separated from the cliff, carrying a portion of one of the build-
ings with it; and altJiongh torn away from the remaining wall, and
thrown over at a considerable angle, yet it remains perfectly firm and
unshaken.
Scratched into the face of the cliff which contains these houses are
various inscriptions, one of which is depicted in Fig. 6 of Plate I. As
they are not cut in very deeply, and in some places mere scratches, it is
very doubtful whether they are contemporaneous with the houses them-
selves.
Two or three miles farther, and the caiion changes in feature again ;
the highest level of the me%a coming forward and towering over the val-
ley with a thousand feet of altitude ; the bottom-lands widening out to
a half and three-quarters of a mile in breadth. Cottonwood and willow
fringe the meandering stream in pleasant groves, while the dead level
of the valley is heavily carpeted with a dense growth of artemisia and
cacti. Everything is dry, dusty, and barren ; the stream itself losing in
volume, and becoming more turbid. Fig. 13 of Plate III represents in
outline the characteristics of the canon, or valley rather, at this point.
In the high bluff, on the right hand in the sketch, are some of the most
curious and unique little habitations yet seen. While jogging along
under this bluff, fully 1,000 feet in height, and admiring its bold outlines
and brilliant coloring, one of our party, sharper-eyed than the rest,
descried, away up near the top, perfect little houses, sandwiched in
among the crevices of the horizontal strata of the rock of which the
bluff was composed. While busy photographing, two of the party
started up to scale the height, and inspect this lofty abode. By pene-
trating a side-caiion some little ways, a gradual slope was found, that
carried them to the summit of the bluff*. Now, the trouble was to ge.t
doicn to the house, and this was accomplished only by crawling along
a ledge of about 20 inches in width, and not tall enough for more then
a creeping position. In momentary peiil of life, for the least mistake
376 GEOLOGICAL SURVEY OF THE TElEtRITORIES.
would precipitate him down the whole of this dizzy height, our adven-
turous seeker after knowledge crept along the ledge until the broader
platform was reached, upon which the most perfect of the houses alloded
to stands. The ledge ended with the house, which is built out flush
with its outer edge. This structure resembles in general features the
cliff-bouses already spoken of. The masonry is as firm and solid as when
first constructed, the inside being finished with exceptional care. In
width it is about 5 feet in front, the side-wall running back in a semi-
circalar sweep ; in length 15, and in height 7 feet. The only aiiertnre
was both door and window, about 20 by 30 inches in diameter. In Fig.
7 of Plate II, is a design of this aerial habitation as it appeared ftom
below, its uniqueness consisting in its position on the face of the hlnS.
To the casual observer, it would not be noticed once in fifty times in
passing, so similar to the rocks between which it is plastexed does it
appear from our position on the trail. A short distance to the right,
and on the ledge above, is another building of somewhat itider con-
struction, but with corners square, and the walls truncated.
Referring again to Plate III and Fig. 13, the position of these booses,
and also of the one in Fig. 12, can be seen in the dark heavy lines near
the summit, just above the most precipitous portion of the blnft, gener-
ally at a height of from 600 to 800 feet alK)ve the level of the canon.
This was the last cliff-house we noticed in this canon. From Uie fiist
to the last, all that were upon an elevation, however slight, were on the
western side of the cafion, with either doors or windows facing east,
overlooking the opposite bluffs. We could' not find even the faintest
vestige of ruins or houses upon the eastern side. Those built low down
on the level land did not hold to the same rule, being scattered indis-
criminately upon either bank of the streajn.
Proceeding down the broad open canon over the now very easy trail,
we espied upon the opposite side of the stream a tower of apparently
greater dimensions than the ones noticed above. The crossing was
execrable; but, forcing a way through the tangled undergrowth to the
stream, a way was found out of it to the ruin some forty rods back ;
(see Figs. 2 and 3.) The tower only remained; this is circular, 1:2
feet in diameter, and now about 20 in height, the wall being about 16
inches in thickness. Facing the valley northward is a window-like
aperture, a.bout 18 by 24 inches in size ; the lower lintel some 7 or 8 feet
above the base. The stones of which it is constructed are uniform
in size and angle. Being so entirely exposed to atmospheric influences,
the mortar has worn away entirely from between the outer layers. In-
side, the debris was heaped up nearly to the window. By referring to
Fig. 3, it will be seen that a rectangular structure, divided into two
apartments, each about 15 feet square, joins the tower. Only one corner
of three or four courses of masonry remains, shown in the sketch by tbe
shaded lines ; the rest being indicated by mound-like lines of loose d&nis^
in which but few stones remain ; from which fact, and also that Uie
center of each square is considerably depressed below the surrounding
surface, it is probable that they are underground apartments, their
roofs not reaching the window midway in the tower. It would be ex-
tremely interesting to excavate upon these old foundations ; for there
is no doubt that many interesting relics, and possibly some clue to their
manner of life, might be found. Our time, however, was too limited to
admit of the experiment, much as we desired the information it might
fnrnish.
In the same neighborhood stands a corner and a portion of a doorway
of a honse, (see Fig. 4), showing considerable care and skill in its con-
m
tJ
Mos] ANCIENT RUINS IN S. W. COLORADO. 377
mction, and what we ba<l not noticed before, the doorway facing east
a little over G feet in height, tall enongh to enable a person to stand
3 in it
With these, we finished our observations of the ruins in the Oauon de
18 Mancos. We were now at its mouth, the mesa ending as abruptly
8 it began: the river turning well westward and following approxi-
lately the course of the San Juan, joins it near the southwestern cor-
.er of the Territory, at the foot of El Late.
Striking off to the right from the stream, and following close under
he bold escarpment of the mesa^ we could still discern, as we bore
iway, group after group of standing walls and mounds, extending down
she valley into thQ broad open plain of the San Juan. It was with
many regrets that we turned our backs upon these relics of a forgotten
race. Our trail now lay over the peculiar marly earths lying under
the sandstones of the table-land, soft, friable, and dusty, without vege-
tation, our mules' feet sinking into it to the fetlocks at each step. At
our right, portions of the mesa have become separated and weathered
into peculiar pinnacled turrets. One particularly stands out detached
some fifty rods; the trail passing between it and the mesa^ forming an
old and well-known landmark on the old Spanish trail from Santa F6
to Salt Lake. A little farther on, and to the right, is another mass,
bearing a curious resemblance to a matron standing with a child beside
her, the alternating bands of red and white strata marking off the fig-
are into its different proportions and into flounces and trimmings.
Away to the south and west, over the broad plains of the San Juan,
where roam the great flocks of sheep and goats belonging to the Nava-
joB, the Callabassas Mountains rear themselves into distinct view ;
while between them and the river, a great cristone thrusts itself up out
of the earth to a height of at least 2,000 feet, as veritable a needle as
was ever christened such.
Striking into this old trail, we bore around to the western side of the
mesa, and, near nightfall, arrived at the extensive group of ruins about
** Aztec Springs," lying out upon the northeastern flanks of El Late,
and close upon the divide between the waters of the Mancos and the
McElmo. It was our intention to have camped here and worked up
the surroundings at our leisure ) but, very much to the surprise of our
guide, the spring was perfectly dry, not even the least moisture remain-
ing to tempt us to dig for it, for others before us had dug to the depth
of three or four feet with no reward for their labor. At its best, it
could have been but a very insignificant source of supply ; the surplus
oozing away through a few yards of wiry grass into the dry sand. The
basin of the spring lay in quite a depression, that had evidently been
excavated for the purpose. A well may have existed ) for it cannot
be reasonably supposed that the very large settlements which at one
time existed in the neighborhood were supplied from it in anywhere
near its present condition. The nearest running water was 12 or 13.
miles away, and none of the surroundings indicated that this spring
ever had any very considerable volume of water. Immediately adjoining
tiie spring, on the right, as we face it from below, is the ruin of a great
massive structure of some kind, about 100 feet square in exterior dimen-
sions ; a portion only of the wall upon the northern face remaining in
its original position. The dShris of the ruin now forms a great mound
of crumbling rock, from 12 to 20 feet in height, overgrown with arti-
misia, but showing clearly, however, its rectangular structure, adjusted
approximately to the four points of the compass. Inside this square is
a circle, about 60 feet in diameter, deeply depressed in the center. The
378 GEOLOGICAL SURVEY OP THE TERRITORIES.
spa^e between the sqaare and the circle appeared, npon a hasty examiii'
ation, to have been filled in solidly with a sort of rubble-masonry. Cross-
walls were noticed in two places ; but whether they were to strength«i
the walls or divided apartments could only be conjectured. That porti<Ni
of the outer wall remaining standing is some 40 feet in length and 15 is
height. The stones were dressed to a uniform size and finish. UpoB
the same level as this ruin, and extending back some distance, were
grouped line after line of foundations and mounds, the great mass of
which is of stone, but not one remaining upon another. AH the sabdi-
visions are plainly marked, so that one might, with a little cai-e, coant
every room or building in the settlement. Below the above group, some
two hundred yards distant, and communicating by indistinct lines of
dSbris^ is another great wall, inclosing a space of about 200 feet square.
Only a small portion is well enough preserved to enable us to judge,
with any accuracy, as to its character and dimensions ; the greater por-
tion consisting of large ridges flattened down so much as to measoie
some 30 or more feet across the base, and 5 or 6 feet in heights This
better-preserved portion is some 50 feet in length, 7 or 8 feetiu height,
and 20 feet thick, the two exterior surfaces of well-dressed and evenly-
laid courses, and the center packed in solidly with rubble-masonry, look-
ing entirely different from those rooms which had been filled with defrm,
though it is difficult to assign any reason for its being so massively
constructed. It was only a portion of a system extending out into the
I)1ains, of much less importance, however, and now only of indistin-
guishable mounds. The town built about this spring is nearly a square
mile in extent, the larger and more enduring buildings in the center,
while all about are scattered and grouped the remnants of smaller struc-
tures comprising the suburbs.
It was sunset by the time we had secured the photographic views
necessary to illustrate the leading features of this group. A camp had
to be found, a thing very easily done in most localities, but here one very
important constituent was wanting. Sage-brush and grass abounded,
but water was sadly deficient. However, by good luck, as we might
call it, a few pools of the grateful fluid were found in the nearly dry bed
of an old stream, about four miles distant from the ruins. This pretense
of a stream known locally as the McElmo, flows westwardly into the
San Juan ; and is for the greater portion of the year but a deep dry
gulch.
A short distance above our camp, and upon the top of the mesa,
which, at this point, is not more than 25 feet above the valley, we
found a tower very similar to that on the Mancos (see Fig. 1), but con-
siderably larger, and surroundec^ by a much greater settlement. It is
about 50 feet in diameter, and, like the Mancos one, double-walled, the
space between the two about 6 feet in width, and subdivided into small
apartments by cross-walls pierced with communicating doors or windows.
. Immediately surrounding this tower is a great mass, of which it is
the center, of scattered heaps of stone d4bris^ arranged in rectangular
order, each little square with a depressed center, suggesting large sab-
divided buildings, similar to the great community-dwellings of the Pue-
blos and Moquis and the old ruins of the Ohaco. Upon the southeast
corner of this group, and upon the very edge of the iite«a,.are the re-
mains of another smaller tower, and below it, founded qpon the bottom
of a small caHon, which ran up at right angles to the McElmo, is ft
portion of a heavy wall rising to the base of this lesser tower. This
group covers a space of about one hundred yards square ; while ad-
joining it on the me%a is group after group upon the same general plau.
WaTCH-TOWEB, IK THK CaSi>S i'f THK McEUMO.
'^
JACKSON] ANCIENT RUINS IN S. W. COLORADO. 379
a great central tower and smaller snrroQDdlDg bnildings. They cover
the whole breadth and length of the land ; and, tarn which way we
. would, we stumbled over the old monnds and into the cellars, as we
mi^ht call them, of these truly aborigines. The same painted, glazed,
and otherwise ornamented ware, of which I have spoken, accompanies
each settlement, and we were continually picking up new designs and
forms.
Starting down the cation, which gradually deepened as the table-land
rose above us, we found upon each hand very old and faint vestiges of
the homes of a forgotten people, but could give them no more atten-
tion than merely noting their existence. Half a dozen miles down,
and we came upon several little nest-like dwellings, very similar to those
in Figs. 5 and 7, bat only about 40 or 50 feet above the valley. Two
miles farther, and we came upon the tower shown in Fig. 9, standing
upon the summit of a great square block of sandstone, some forty feet
in height, detached from the bluff back of it. The building, ux>on its
summit, is square, with apertures like windows upon two faces, looking
east and north, and very much mined, but still standing in some places
about 15 feet above the rock on which it is built At the base of the
rock is a wall running about it, a small portion only remaining, the rest
thrown down and covered with dSbris from the house above.
About here we crossed the boundary-line into Utah, and then, tvvo
or three miles farther, we came upon a very interesting group. The
valley, at this place, widens out considerably, and in the center stands
a solitary butte of dark-red sandstone, upon a perfectly bare and smooth
floor of the same, dipping down to the center of the valley at a slight
inclination. The butte, a remnant of a former mesaj worn down by
time to its present dimensions, is about 100 feet in height and 300 in
length; an irregular mass, seamed and cracked, and gradually going
the way its former surroundings have traveled. Banning about its
base, in irregular lines, are remains of walls, but whether for defense or
habitation would be hard now to determine. At the back of the rock,
a view of which is had in Fig. 10, are the remains of two quite consid-
erable walls, one above the other; the lower portion — one corner only of
a square building, all traces of the remaining portions having entirely
disapp)eared — seemed to serve as a sort of approach to the larger build-
ing above, the top of which came up nearly to the summit of the rock.
It is about 18 feet in length and 12 feet in height. Portions only of the
side-walls, connecting it with the rock, remain. The stones of which it
is built are very uniform in size, angle, and finish, more so than any yet
seen, but, like all similarly-exposed buildings, the mortar is washed or
worn away entirely from between the outer layers; farther in, it is
intact as usual. In front is a single aperture of about 18 by 24 inches,
whether for door or window would be hard to guess. The only access
to the top of the rock was through the window of this house. On top
are evidences of some sort of mason-work, that covers it from one end
to the other. All the irregular gaps and crevices have been walled up,
probably to make an even surface. But few of the stones remain in
position ; in one or two places, three or four courses, all the rest are
thrown down and scattered.
In the rear, about fifty yards removed, are other ruins belonging to
the group, surrounding the rock. The better-preserved portions consist
of a square tower, with one round comer, about 12 feet in diameter, and
upon the lowest side — which stands in a dry run— rabout 20 feet in
height. The walls are 18 inches in thickness with no signs of apertures.
Adjoining this ruin is another, but so much thrown down as to be almost
380 GEOLOGICAL SURVEY OP THE TEBBITORIES.
unrecognizable ; and between these and the Fock were circular depres-
sions ot some considerable depth, indicating either subterranean ap^rt-
meuts or reservoirs. No water could be found anywhere in the neigh-
borhood. The dry bed of the McElmo was fully a mile distant, in wbidi
water occurs during the winter and spring only.
Aside from the interest attaching to the ruins themselves, there are
thrown about this rock and its surroundings the romance and charm
of legendary association. The story runs thus, as given us by oar
guide, and very excellently rendered by Mr. Ingersoll, in his article to
the New York Tribune of November 3 :
Formerly, the aborigiDes inhabited all this country we bnd been over as far west as
tbe headwaters of the Sau Jaan, as far north as the Rio Dolores, west some distance
into Utah, and soath and southwest throughout Arizona and on down into Mexico.
They had lived there from time immemorial — since the earth was a small island, which
augmented as its inhabitants multiplied. They cultivated the valley, fashioneil what-
ever utensils and tools they needed very neatly and handsomely out of clay and
wood and stone, not knowiug any of the useful metals ; built their homes and kept
their flocks and herds in the fertile river-bottoms, and worshiped the sun. They
were an eminently peaceful and prosperous people, living by agriculture rather than
by the chase. About a thousand years ago, however, they were visit-ed by 8av>
age strangers from the North, whom they treated hospitably. Soon these visits
became more frequent and annoying. Then their troublesome neighbors — ances-
tors of the present Utes — began to forage upon them, and, at last, to massacre
them and devastate their farms ; so, to save their lives at least, they built boaaes
high upon the cliffs, where they could store food and hide away till the raiders
leu. But one summer the invaders did not go back to their monntaiuR as the people
expected, but brought their families with them and settled down. So, driven from
their homes and lands; starving in their little niches on the high cliffs, they could only
steal away during the night, and wander across the cheerless uplands. To one who
has traveled these steppes, such a flight seems terrible, and the mind hesitates to pic-
ture the suffering of the add fugitives.
At the cristone they halted, and probably found friends, for the rocks and caves are
full ot the nests of these human wrens and swallows. Here they collected, erected
stone fortifications and watch-towers, dug reservoirs in tbe rocks to hold a supply of
water, which in all cases is precarious in this latitude, and once more stood at bay.
Their foes came, and for one long month fought and were beaten back, and retnnied
day after day to tbe attack as merciless and inevitable as the tide. Meanwhile, tbe
families of the defenders were evacuating and moving south, and bravely did their
protectors shield them till they were all safely a hundred miles away. Tbe besiegers
were beaten back and went away. But the narrative tells us that the hollows of the
rocks were filled to the brim with the mingled blood of conquerors and conquered,
and red veins of it ran down into the cafLon. It was such a victory as they could not
afiord to gain again, and they were glad, when the long fight was over, to follow their
wives aud little ones to the south. There, in the deserts of Arizona, on well-nigh un-
approachable isolated bluffs, they built new towns, and their few descendants, tbe
Moquis, live in them to this day, preserving more carefully and purely the history and
veneration of their forefathers than their skill or wisdom. It was from one of their old
men that this traditional sketch was obtained.
The bare floor of nearly white sandstone, upon which the butte stands,
is stained in gory streaks and blotches by the action of an iron constit-
uent in the rocks of another portion of the adjoining bluffs, and this
feature probably gave rise to the legend. Half a mile back, or north
from this historic butte, is a group of small cave-houses. A long bluff
line, about 100 feet in height, of alternating bands of red and white
sandstone, has, along a line of its upper'strata, quite a number of shal-
low caves, in which are snug little retreats, securely walled in, the
masonry perfect and substantial. Along the top of the bluff are traces
of old walls, but now well-nigh obliterated.
While passing the mouth of a wide uide-cafion, coming in from tbe
right, a tall, black-looking tower caught our eye, perched upon tbe very
brink of the mesa, overlooking the valley. Tying our riding-animals at
the foot, and leading the pack-mule^ with photographic kit, we soou
JACK80K.] ANCIENT RUINS IN 8. W. COLORADO. 381
strack into an old trail, worn deep ioto the rocks, winding and twisting
among great bowlders, and overgrown and obstructed with rank growth
of sage, cedar, and cacti. In its day, the trail had been a good one ;
now it was anything bat such. Bad as it was, however, it was the only
way to the snmmit, and we were thankful for it. Skirting the edge of
the mesa a few yards, we came to the tower, the trail passing back of it
and on up to a higher level. A huge block of sandstone has rolled down
frona the escarpment of the mesa above, lodging upon the very brink of
a bench midway between top and bottom, and upon this the tower is
built, so that from below both appear as one. They are of the same
diameter, about 10 feet, and some 18 feet in height, equally divided be-
tween rock and tower. In construction, it is similar to those already
described, of single wall. It was evidently an outpost or watch- tower,
gaarding the approach to a large settlement upon or beyond the mesa
lying above it. From this point we now struck out for another group
of ruins lying upon a nameless stream, some eight or ten miles farther
west. Four or five miles we followed the McElmo down, the trail good,
the whole surface covered with a dense growth of artemisia and groves
of eedar and pinon, with cottouwoods fringing, the dry stream. Branch-
ing off at right angles, crossing the heads of two caiions which o[>ened
out quickly into great gorges, and then descending into a valley densely
covered with greasewood, we came upon the ruins we were in search of.
Through the valley ran a deep gulch, a narrow thread of warm, brackish
water appearing at intervals in its bed, and gathering into pools in
basins a short distance below the ruins.
In Fig. 11 of Plate III, is a sketch of a ground-plan of the ^^ city,"
showing its general arrangement. The stream referred to, and shown
in the sketch, sweeps the foot of a rocky sandstone ledge, some 40 or 60
feet in height, upon which is built the highest and better- preserved por-
tion of the settlement. It« semicircular sweep conforms to the ledge;
each little house of the outer circle being built close upon its edge. Be-
low the level of these upper houses some 10 or 12 feet, and within the
semicircular sweep, are seven distinctly-marked depressions, each sepa-
rated from the other by rocky d6l>ris\ the lower or first series probably
of small community-houses. Upon either flank, and founded upon rocks,
are buildings similar in size and in other respects to the large ones on
the line above. As paced off, the upper or convex surface measured 100
yards in length. Each little apartment is small and narrow, averaging
6 feet in width and 8 feet in length, the walls being 18 inches in thick-
ness. The stones of which the entire group is built are dressed to nearly
uniform size and laid in mortar. A peculiar feature here is in the round
corners, one at lea«t appearing upon nearly every little house. They are
turned with considerable care and skill, being true curves solidly bound
together.
With this last our observations of these interesting relics came to an
end. Our trip was short and rapid, and instituted in the first place, as
I have said, in quest of the picturesque, and we found it. For a much
more complete and faithful exposition of this interesting subject, the
reader is referred to a series of photographic views from which the ac-
companying illustrations are drawn.
I cannot close without extending thanks to Gapt. John Moss, of La
Plata, our volunteer guide, who accompanied us over the route compris-
ing the ruins. To his accurate knowledge of their locality, and the best
way to reach them, aa well as of the language of the Indians, is due much
of the success of the trip.
ZOOLOGY.
REPORT OF ERNEST INGERSOLL
-■< ,
{
REPORT ON THE NATURAL HISTORY OF THE UNITED STATES
GEOLOGICAL AND GEOGRAPHICAL SURVEY OF THE TERRI-
TORIES, 1874.
By Ernest Inobrsoix, Zoologist.
New York, March 1, 1876.
Sis : I herewith forward the subjoined report of zoological work done
during the season of 1874 in connection with the survey ander yoar
direction, a preliminary account of which was published by you in the
Bulletin of the Survey, second series, No. 2, under date of May 14, 1875 ;
and I remain, with high respect, yours, etc.,
ERNEST INGERSOLL,
Zoologist
Dr. F. V. Hayden,
27. JS. Oeologisty Waskington^ D. (J.
The material herein reported upon consists of two collections, chiefly
of moUusks: one made by Mr. E. A. Barber, of West Chester, Pa., in the
northwestern part of the Territory ; and the other made by the writer
in connection with the Photographic Division of the Survey during July,
August, and September of 1874, in which he was assisted by Master
Frank Smart, of Washington.
Mr. Barber was attached to Mr. Marvine's Topographical Party, and
collected plants and shells in North Park, along Bear and White Rivers,
and at the White River agency, where he was engaged in making baro-
metric observations for several weeks. His collection is not large, but
is interesting in that it exhibits several species which I did not find,
and also includes additional examples of the new Microphysa^ which was
described by Mr. Bland from my specimens.
My own route lay from Denver west into Middle Park, thence sonth
up the valley of the Blue to Hoosier Pass, leading the party into South
Park, from which we crossed over to the Arkansas, and thence through
Poncha Pass into San Luis Park, and across to Saguache. From here
the road led west to the Los Pinos Indian agency, and then southwest
through Antelope Park to Baker's Park, in the high mountains.
At this point, the camp was stationed ; and leaving Mr. Smart to col-
lect here, I accompanied Mr. Jackson on a side-trip of nearly three
weeks' duration, made southwest into the valley of the Rio San Juan,
at the extreme corner of the Territory. On our return trip from Baker's
Park, we followed the Rio Grande to Del Norte, thence struck across
the San Luis plain to the ^^ sand-hills," through Mosca Pass, Huerfano
Park, Wet Mountain Valley, and Oak Greek, and finally came to Ganon
Gity, where 1 left the party.
Gollections were made at nearly every camp on the whole route, and
that they do not make a greater aggregate is due to the ihexperience of
the writer, the haste with which the party moved, and not a little to the
comparative scarcity of those objects in which he happened to take the
most interest, and most desired to have completely represented. In
such cases, in the absence of specimens or affirmative evidence, a oer*
38&
25 H
386 GEOLOGICAL SURVEY OF THE TEBBITORIES.
taiD amoaDt of negative evideDce appears, which may be of valae in
future deductions. I append a list of the localities, remarking npon ele-
vation and <8o forth, at which collections were made. The absence of
any camp, as Nos. 12-16, from this list, does not necessarily imply that
I was idle, bat that nothing of importance reached home from that
locality.
LIST OF LOCALITIES FROM WHICH SPECIMENS WERE BROUGHT HOME.
Camp 9 : Hot Sulphur Spring^^ Middle Parky July 31 to August 5. Ele-
vation 7,725 feet. A broad, open valley, containing hot and cold
springs of various mineral- waters.
Camp 9-10 : Orand River Valley, August 5. About 7,600 feet Grassy
prairies and river terraces of coarse gravel covered with sage-brusb,
with but little timber, except along some portions of the river-banks.
Camp 10 : Mouth of Blue River y Aqgust 6-8. About 7,600 feet. High
river-terraces. Cottonwoods and alders along the river and about
springs in the neighboring hills.
Camp 10-11 : Blue River Valley^ August 8. 7,500-8,500 feet. Same
general characteristics.
Camp 11 : Ute Pealc^ Blue River Yalleyj August 8. About 8,500 feet
Springy ground by a cold streamlet, with abundance of small timber
and luxuriant herbage. Many shells were collected on a wooded hill
2,000 feet higher than the camp.
Camp 17 : Head of San Luis Valley^ August 14. About 8,000 feet
Luxuriant grass and herbage ; large pines and spruces. Water in
plenty.
Camp 17-18 : San Luis Valley, August 15. 7,600-7,200 feet Distance
thirty miles, mo&tly Artemisia plains, very dry and dusty. The weather,
which had been rainy, now began to be clearer, with hot noondays
and cool nights.
Camp 18 : Springs^ Saguache, August 16. 7,700 feet. Edge of dry plains.
The springs come copiously from under a volcanic bluff, and flow into
a marsh, which drains into Saguache Creek.
Camp 19 : Saguache Creeks August 16. 7,748 feet Five miles beyond
Camp 18, on the banks of the above stream, which, is a tributary of
the Bio Grande and waters a fertile region. Thousands of cattle are
herded hereabouts.
Camp 20 : Twenty miles west of Sagua^chcy August 17. About 9,000 feet
Volcanic canon.
Camp 21 : Los Pinos Indian agency j August 19-24. 9,290 feet. A fer-
tile plain watered by two creeks, and surrounded by hills, affording
plenty of rain. The camp was placed among a grove of various trees
by a little rocky stream. We remained a week at this point; but my
time was largely occupied in studying the traits of the Ute Indians,
whose southern agency is here.
Camp 22 : White Earth Creek, August 24. About 8,000 feet A deep
ravine, which had been recently burned over.
Camp 23 : Timber line; divide .between the Gunnison and Rio Orande, Au-
gust 25. About 10,000 feet Timber mostly small ; no pines. Found
many mollusks in the deep wet grass early in the morning.
Camp 24 : Clear Creek, August 26. About 9,300 feet A tributary of the
Bio Grande, emptying in Antelope Park. The banks were here cov-
erad with a riotous growth of brush and weeds.
GAJfP 26 : Jennison^s Ranch, August 27-28. About 9,600 feet On the
Bio Grande, between Antelope and Baker'a Parks. Fertile alluvial
JHOEBSOLL.] ZOOLOGY — ^LIST OP LOCALITIES. 387
bottoms, with pleuty of timber on the hills. Clear, wirh frosty
nights.
Camp 26 : ffotcardvillej Baker^s Park, August 29-September 23. 9,709
feet. A deep valley among immense trachyte mountains. Abundance
of timber (spruce and the like, and aspen), bushes and plants. Frosty
nights, and snow toward the last of our stay.
Cunningham Quick is a deep canon liearby, on the high, perpendicular
side of which, aloug trails leading to silver-mines, I found active mol-
lusks and insects at an altitude of fully 1.1,000 feet.
Camp D: Cascade Creek; head of the Animas Valley, September 3.
About 8,000 feet. Southern slope of high sierras. A beautiful region
in all respects. This and the four following localities were on the
side-trip into the San Juan Valley.
CampE: Animas Park, September 4. About 6,600 feet. Lower down
the river, where the broad bottoms are somewhat cultivated.
Camp E-F : Betvceen the Rio Animas and Rio La Plata, September 4.
8,000 i'eet. Half-way we passed a great poud, surrounded with rushes ;
the resort of innumerable wild fowl, and inhabited by a great variety
of fresh-water life. Observe the note to Selisoma trivolvis.
Camp F : Rio La Plata mining-camp, September 6-8. About 7,500
feet. Collections made in dense damp groves of evergreen and de-
ciduous trees.
Camp K: Hovvenweep, Utah, September 13. About 4,500 feet. Alow,
dry ravine some twenty miles into Utah, in a desolate mesa country,
named by us Hovvenweep, from two Indian words meaning deserted
caiion. Only gnarled cedars, sage-bush, and greasewood grow there.
The valley must be subject to floods.
Camp P : Head of Mineral Creek, September 19. About 10,000 feet. The
sources of a mountain-torrent draining into Baker's Park.
Camp 28-29: Saint Mary's Lake, Antelope Park, September 25. 9,300
feet. A beautiful lake without inlet or outlet, on the northeastern
side of the park, surrounded by rocky cliffs. Inhabited by some pe-
culiar shells and hosts of water-fowl, while its shores are the resort of
large herds of antelope.
Camp 30 : Rio Orande above Del Norte , September 28. 7,660 feet The
camp was in a low spot by a sluggish stream.
Camp 32: Lakes, San Luis Valley, September 20. About 7,600 feet.
These lakes are most of them dry in September, and all the shells I
found were dead on the beach. They are frequented by innumerable
wild geese and ducks, which are tormented by the many large gulls
which make the lakes their home. The waters are alkalinei^ and the
whole region is white with saline deposits and nearly barren.
It will be observed that all of these localities are in Colorado except
Camp K.
aElTEEAL AOOOUNT OP THE WORK,
Attention was chiefly given to firesh-water invertebrate life, though
the results were not very satisfactorj'.
At the springs near Saguache, leeches were found, pronounced by
Prof. A. E. Verrill to be Aulostomum lacustre, vaPi tigris, Verrill, and
Cl^sine modesta, Verrill, both of which have been fouod heretofore in
the same region. A more thorough search, had it been possible, would
probablv have revealed additional forms, as the locality was extremely
lavorable.
For Crustacea a sharp lookout was kept, but only the following spe-
cies were certainly seen : two amphipods, Oammctrus robustus, Smithy
388 GEOLOGICAL SURVEY OF THE TEBSITOBIES.
aud Hyallela inermiSy Smith, both of which were described in the Report
for 1873, which inhabited the above springs in great abundance. From
the pond mentioned between camps E and F a small crab was bronght
home, which Prof. S. I. Smith pronounced to be a true marine form, be-
longing to the Astacidoas, That this is a survivor of the period, probably
comparatively recent, when this pond was a salt-water marsh, is sap-
ported by the astonishing fact that two specimens of a young Trui^
catella aud well-preserved fragments of an Arcd were found on the
muddy shores. It would be of great interest to know whether the
exuberant vegetation of the pond retains any traces of marine plants.
The insects w<^re not methodically collected, and but few, chiefly my-
riapods, which are very abundant in the mountains, were brought home.
A small collection of spiders consists of ten species of Arane^ {Dras-
gidcc 2, Lycosa 5, Aitus 1, Tfiomisus 2) and four species of Phalamgejb
(PhalangeinSj Oonyleptes 1). All of these species are believed by Mr.
£. H. Emerton, who has examined them, t6 be undescribed, though iti
part identical with forms previously collected in Colorado. A descrip-
tion is not attempted herewith, because the material is not at hand for
proper study and comparison. Further collections and observation in
this branch of entomology are particularly desirable from the mountain-
ous regions of all the Territories.
Land and fresh- water shells comprise the largest part of the material
brought home. They were made a specialty ; and the fact that next to
nothing of this class had ever been reported from Colorado, and but lit-
tle was known at all of the Mollnsca of the Bocky Mountain region, was
deemed a sufficient excuse for what might seem too exclusive attention
to this department of natural history, which does not present to the
careless mind such striking attractions as the study of the higher ver-
tebrates.
No fishes were collected, although numerous attempts were made.
The majority of our time was spent where they seemed to be entirely
absent, or so extremely scarce that, although all were interested in tbe
capture of certain species, not a trout graced our table during the
whole trip.
Some snakes and frogs were secured at Hot Springs, Middle Park,
aud a number of AmblyHtoma seen for the first and last time. Beptiles
were taken wherever they occurred after this, also, except upon tbe
long side- trip mentioned above, where it was impracticable to preserve
anything greater than could be put in a pocket-bottle of alcohol. The
marsh between the Animas and La Plata was a fine locality for batra-
chians. South of the mountains, lizards began to appear in great num-
bers and variety, and increased as we got farther out upon the dry
plains. Camp 20 furnished us our only rattlesnake, and I do not
remember any other camp at which we were even suspicious of their
presence.
Such large suites had already been secured of the mammals and birds
of Colorado that it was not deemed advisable to spend time in a syste-
matic collection of them. Some skins were obtained, and observations
recorded, but little worthy of special mention. Birds were nowhere
seen so abundantly as in Berthoud Pass and on the Arkansas below
Granite. The former locality, being easily accessible, ought, before
many seasons, to yield a rich ornithological harvest.
In conclusion, I wish to express to Mr. Wm. H. Jackson, director of
our party, the appreciation I have of his hearty co-operation and genial
sympathy, through which he not only afforded me opportunities I would
not otherwise have had, but added immensely to my personal enjoy-
ment of this delightful trip.
SPECIAL REPORT ON THE MOLLUSCA.
The collection of Mollnsks fairly represents the land and fresh-watier
families, and comprises many additions to the fauna of Colorado, as well
88 the following six species, believed to be new :
Idmoj^^mantanuSy Ingersoll.
lAmax castaneusj Ingersoll.
Microphysa IngersoUi^ Bland.
Pupilla alticolay Ingersoll.
Helisoma plexata^ Ingersoll.
With respect to their distribntion, it will be seen that none were found
on the eastern slope of the rantr(*, although there is no conclusive evi-
dence that they do not exist there; Ibat there was a marked increase
as we advanced south; that altitude seemed to have little influence
upon their range so long as other favorable conditions were present ;
and that some species (as of Eelisoma) had a very local distribution.
The genera Zonites, Vitrina, Vallonia, Pvpa, Sucdnea^ and Pisidium
were widespread. Among the Helices, Paiula Cooperi only occurred in
broad open valleys; Paiula striatella and Cronkhitei were found together
over the northern portion of the district traversed, but in the south the
latter replaced striatella. The little Microphysa, occurring abundantly
on the cliffs in Baker?s Park up to 11,000 feet, and in the Animas and
other valleys draining into the Bio San Juan, was also found in the North
Park by Mr. Barber, but his examples were less robust. All the other
species of this genus belong to Florida and the Gulf coast. The Pupas
were perhaps the most common forms, increasing as we went south,
where specimens of Vertigo californica and Pupilla alticola were numer-
ous everywhere on the mountains as high up as timber grows. Pupilla
Blandij heretofore known only as a fossil in Missouri River Drift, was col-
lected alive in considerable numbers.
In order to make this Ist as far as practicable a stateuient of our
present knowledge of the Mollusca of that portion of the United States
lying between the Bocky Mountains on the east and the Sierra Nevada
on the west, designated, by Mr. W. G. Binney, Tfie Central Province
(Bulletin Mus. Comp. Zool, III, ix), I have inserted in their proper system-
atic place the niimes of such mollusks as I could ascertain to have
occurred within that region, distinguishing those species which form
my own list by the black head-letter type. A brief mention of the
range extralimital to the scope of this paper is added to most species.
There seems some reason to doubt whether the limits assigned by Mr.
Binney in his Geographical Catalogue, above referred to, circumscribe
a true zoological province, considered with reference to the Mollusca;
but I have contented myself with carefully tabulating such observations
as I had access to, leaving to others such deductions as the facts may
warrant. Enough is presented, however, it seems to me, to show that the
Central Province, so-called, is not so deficient as has been supposed,
either in the number of species or in representiitives of adjoining faunas.
The impression that this inter- montanic region is unfavorable to the
development of Pulmouates also seems wrong, except in respect to the
scarcity of lime, to which cause we may probably attribute the fact that
the more minute forms are in large majority. A further discussion of
the geographical and hypsometric distribution of the Moilusks of the
389
390 GEOLOGICAL SURVEY OF THE T£RRIT0R1£8.
liocky Moniitaiugi may be found in an article by the author iu the Popular
Science Monthly lor May, 187(J.
It gives me pleasure to acknowledge my indebtedness and tender my
thanks to Messrs. Thomas Bland and W. G. Binney, Dr. James Lewis
aiid Prof. Edward S. Morse, for much kind help and good counsel, boA
before and after the completion of this manuscript.
moLiiVscA.
Class GASTEROPODA.
Order PECTINIBRANCHIATA.
Family VALVATID^B.
Valvata siaceia, Say.
•
Lakes ; San Luis Valley 1 specimeo.
lleported also from Salt Lake (Hetnphill). Inhabits the Western
States.
My single shell was found dead upon the beach. It is typical, except
in size, which exceeds that of any other specimens I have seen. I agree
with Mr. W. G. Binney that I have never seen " specimens referred to
this species that can easily be distinguished from carinate forms of
F. triearinataJ^
Valvata virensy Tryon. — Cceur d'Al^ue Lake, Montana {Hemphili ) ;
Pacific coast.
RISSOID^iE.
AMNICOLIN^.
Tryonia clatliarata, Stm. — Colorado Desert (Blake),
Tryonia protea^ Gld. — Colorado Desert {Blake.)
Somatogynis iBOg^onns Var. subglobosus, Sat.
Lakes ) San Luis Valley .\ • 5 specimenB.
Northwestern part of the Union {Say).
All my specimens were dead. My time was so limited at this inter-
esting point that I could not search the deep water for living moliusks.
Amnicola turbiniformiSj Tryon. — Crane Lake Valley and Surprise Val-
ley, Northeast California {Gabb)-, near Fort Hall, Idaho {Eeid)-, Truck-
ee, Nevada {Carlton). California.
Amnicola longinqua^ Gld. — Colora<lo Desert {Blake).
Fluminicola Nttttalliana, Stm. — Warm Springs, near Salt Lake^Utah
{Beid) ; Upper Des Chutes River, and Klamath Eiver, Oregon (New-
berry). Oregon and California.
Fluminicola seminalis, - Stm. — Salt Lake, Utah {B€id)'j Oregon and
Washington Territory (Newberry).
Fluminicola Eindm^ Stm. — Salt Lake, Utah (Beid) ; River Kootaiiie
and stream at foot of Rocky Mountains, 4,G2G feet, British Columbia
(Lord).
IKGER80LL.] ZOOLOGY ^MEL ANIIDiE — ^PULMONATA. 391
The la8t two of these three species are considered identical with the
first by Mr. Binuey and some others ; their range seems to be co-exten-
sive.
Fluminieola fusca^ Hald. — Shores of Lake Utah [Burton) ; Sacramento.
Biver, California, to Green Biver, Utah (Cooper),
< «
POMATIOPSIN^.
Pomatiapsis intermedia^ Trvon. — Owyhee River, Southeast Oregon
{Qahb)) White Pine district, Nevada {Hemphill), Pacific coast.
MELANIID^,
Choniabasis pliciferay Lea. — Rivets of Washington Territory (Cooper),
Pacific coast.
Ooniabasis siliculay Gld. — Usually regarded as a variety of the above.
Quoted from Washington Territory ; Oregon ; Hell Gate River, Mon-
tana ; and the Missouri above the Falls (Cooper). Pacific coast.
Ooniabasis Newberryi, Lea. — Upper des Chutes River, Oregon (Neic-
eofnb), California.
Ooniabasis nigrina. Lea. — Clear Creek, Shasta County, California.
Pacific coast.
Ooniabasis Draytoni^ Lea. — Walla Walla, Oregon; Clear Creek, Shasta
County, California. Pacific coast.
Leptoxis fuscay Hald. — Shores of Lake Utah (Burton). Pacific coast.
Order PULMONATA.
PUPID^.
PUPlN-ffl.
Cumella sabcylindrioa, Linn^us.
C^mp 24 : Clear Creek 3 specimens.
These three were found in wet grass and bushes, some 8,300 feet above
the sea. Though I searched particularly for them afterward, no more
were obtained. It is a circumpolar species.
Pnpillainiisconun, LiNN^us.
Camp 11 : Blue River Valley 1 specimen.
Camp 21 : Los Pinos Agency 5 specimens.
Canada ; Eastern States ; Europe.
Papilla Blandi, MoBSE.
Camp 24 : Clear Creek 2 specimens.
Camp 26 : Cunningham Gulch 40 specimens.
Camp D: Animas Valley 1 specimen.
Camp F : Rio La Plata 1 specimen.
Sub-fossil in Drift on Missouri River near Fort Berthold.
Pnpilla altioola, sp. noy.
Animal not observed.
Shell perforate^ straight, tito and one-half times as long as broad, densely
striate, subtran^tlucenl^ chestnut-brown ; apex obtuse ; xchorls 6 or 7, convex,
392 GEOLOGICAL SURVEY OF THE TESBIT0B1E8.
the middle three of the apire equal, cawting a paralleJUm in the sidet of the
shell, the last noticeai>ly greater, expanding toward the aperture, not closely
appressed to ttte body-vhorl; suture deeply impressed; aperture smaH,
oblique, subtriangvlar, margins connected bg a thin deposit, without internal
processes; peristome simple, somewhat reflected over theumbilicus. Length,
33 mm. ; diameter, 1 mm.
Cnmp 26 : Canningham Oalch 25 Bpccimens.
Gamp F: Bio Ita Plata.. _ 5 Hpecimeas.
It vill not be difficalt to recognize tbia apeciee b; its parallel sides,
base-like expaDsion of the laat wborl, coarse iiicrenieotal lines, ami eden-
tate aperture. It fleeiua to be an eBseotially alpine species, none having
been fouud at an elevation leea tbaa 8,000 to 9,000 feet. It was plenty
in the localitiea mentioned above.
Leucochila arvsonensis, Gabb. — Fort Grant, Arizona {Horn); Pike's
Peak, Colorado (IVyon); White Pine, Nevada (-H«Mj>ftt»). Calitoruia.
Leucochila hordea^eOj Oabb. — Fort Grant, Arizona (Horn).
TBBTiaiNlN^.
Vertigo califomioa, Bowell.
Campll: Bine Eiver Valley 15 specimens.
ramp21: Los Pi noB agency 3 specimens.
Camp 23 : Divide aouth west of Los Finos 3 specimens.
Camp 26: Howardville 50 specimens.
Camp D : Animaa Valley 2 specimens.
Camp F: Bio La Plata 4 8i)ecimens.
Pacific coast.
Vertigo Gorpnlenta, MoBSE.
Camp 21 : Los Pinoa agency 2 specimens.
Camp 23 : Divide sonthwest c' Los Pinoa 1 8i>ecimen.
Eastern slope Sierra Nevada (Stretch; Hemphill),
Vertigo ovata^ Hay. — Fort Grant, Arizona (teste BiuTiey). Eastern
United iStatea.
HELICID^.
VITEmJE.
Macrocyclis vancouverensis, Lea. — Idaho; west side of Ctenr d'Al^ne
Mountains, in foreata of Couiferse { Cooper) ; Suniass Prairie, Fraser Kiver
[Lord). PaciHc coiiet.
Zonltes arboreaa. Say.
Camp 9: Hot Sulphnr Springs 3 specimens.
Campll: Bine River Valley ]3 specimens.
Camp 26: Howardville, Baker's Park 22 specimens.
Camp F: Bio La Plata 3 specimens.
North Park {Barber) 2 specimena
woEMOLL.] ZOOLOGY — ^HELICID^. 393
»
^^Damp bottom-lauds along the lower valley of Hell-Gate Biver, Mon-
tana" (Cooper); Washoe (Joauty, Nevada; Montana; Bio Chama, New
Mexico {Binney and BUmd). United States generally.
Zonites viridnliu, Menkb.
Camp 11 : Blue Biver Valley 2 specimens.
Camp 19 : Saguache Greek 12 specimens.
Camp 20 : Twenty miles west of Saguache 1 specimen.
Camp D : Cascade Greek, Animas Valley . r 3 specimens.
CampF: Bio La Plata....* 4 specimens.
1 find no other localitieSifor this mollusk recorded in the inter-montanic
region, except that Mr. Lord mentions fiuding a '^ Ztmites like electrina^
Fort Golville, Columbia Biver "; and Mr. Binney accredits it to the
Central Province. All my own localities were at the foot of mount-
ains, and in each case the animals were found in the wet shaded ground
beside running water. In the valleys of the Animas and La Plata, they
were very abundant under logs. It is distributed over the United States
generally, except on the Pacific coast.
Zonites indentatm^ Say. — Accredited by Mr. Binney (Bull. Mus. Gomp.
Zool., Ill, ix, 202) to the* Central Province (Utah) as having been de-
rived from the north. Eastern North America.
Zonites nitiduSj Miill. — Colorado (Carpenter), Europe, New York,
Ohio, and British America.
Zonites Whitneyij Newc. — Lake Tahoe, Sierra Nevada, 6,100 feet
(Cooper); Truckee, Nevada (CarWon).
Zonites Breweri^ Newc. — Truckee, Nevada (Carlton); Lake Tahoe
(Newcomh). California coast.
Zonites minusculus, Binney. — Accredited in Biuney's catalogue to the
Central Province ; Fort Grant, Arizona (Horn). All of North America
and the West Indies.
Zonites conspectus, Bland.
Camp 26 : Cunningham Gulch, altitude 11,000 feet 1 specimen.
No mention has been made of this species that I am aware of since
its description by Mr. Thomas Bland (Ann. N. Y. Lye. N. H., VIII, 163),
who quotes San Francisco, California, a« its habitat.
Zonites ftdvns, Dbapebnaitd.
Camp 9 : Hot Sulphur Springs 5 specimens.
Camp 10 : Mouth of Blue Biver 5 specimens.
Camp 20 : Twenty miles west of Saguache 2 specimens.
Camp 24 : Clear Creek 35 specimens.
Camp 26 : Howardville, Baker's Park . 25 specimens.
Camp D : Animas VWley 10 specimens.
Camp F : Bio La Plata - 6 specimens.
Camp P : Head of Mineral Greek 25 specimens.
North Park (Barber) 6 specimens.
Found heretofore in the White Pine district (Hemphill) and Truckee
Valley (Carlton) of Nevada; and at Lake Tahoe (Cooper). North Amer-
ica, and boreal regions generally.
The specimens vary in size and proportion, many being young. The
highest localities, it will be noticed, yielded the greatest number of
specimens, as Camp 24 (9,300 feet), Camp 26 and Camp P (10,000 feet).
394
GEOLOGICAL SURVEY OF THE TERBITOBIES.
Vitrina limpida, Gould.
Camp 24 : Clear Creek, Northeast Antelope Park 25 specimens.
Camp 26 : Howardville, Baker's Park 3 specimens.
Camp D : Auimas Valley 12 specimen&
I do not find this species anywhere recorded from the central basin.
It was, therefore, after long hesitation that I separated these specimens
from the following species, which inclades the majority of the Vitruut
collected, and has a co extensive distribution in. the Rocky Mountain&
The recorded range of the present species is eastward from Lake
Superior.
Vitrina Pfbifferi, Newgomb.
Camp 21 : Los Pinos agency 25 specimens.
Camp 23 : Divide southwest of Los Pinos 15 specimens.
Camp 26 : Howardville, Baker's Park ^ 40 specimena
Camp F : Rio La Plata 4 specimens.
Camp P: Head of Mineral Creek ^ 6 specimens.
Carson Valley, Nevada {I^ewcomb); Lake Tahoe (Cooper); head of
Gunnison River, Colorado (Carpenter). Western slopes of the Sierra
Nevada.
It whl be noticed that all my localities are sonthem, but at a great
elevation, shells from Mineral Creek having been collected in a snow-
storm. It is well known that '^ the animal is very hardy ; for, according
to Nilson, it is found crawling about among leaves in the southern part
of Sweden in the depth of winter, and it is also found in the most north-
ern part of that country." The gentlemen of (he United States Explor-
ing Expedition found their specimens of Vitrina almost universally on
the tops of mountains.
Limax montanns, sp. t^oy.
Color hluvshgray ; form stouty with blunt posterior extremity; length
exceeding one inch ; color hrown^ ucith mantle^ headj tentacles and cye-pedun-
eles black ; bottom of foot white.
If Jaw. 2, Lineal dentition. 3, Genitalia: a, external orifice; (, genitnl bladder;
c, ovidact; d, testiole; e, epididymis ; f, ovary; §, vas deferens ; a, penis-aao.
uroERsoix.] ZOOLOGY — HELICID^. 395
Jaw as nsual in the genus. Lingual membrane long and narrow.
Teetlx 50-1-50, with 16 perfect laterals. Centrals with base of attach-
ment slightly longer than wide; inferior lateral angles not much pro-
duced, lower margin incurved; reflection slightly shorter than one-half
the base of attachment ; tricuspid, the outer cu^ps short, stout, bearing
short, stout cutting-points ; the median cusp stout, reaching almost to
the lower edge of the base of attachment, beyond which projects the cut-
ting-point; laterals like the centrals, but unsymmetrical, as usual, by
the suppression of the inner cusp with its cutting- point and inner lower
lateral expansion of the base of attachment. There are 16 perfect lateral,
beyond which are several teeth, forming the usual gradual transition to
the marginals. These latter are aculeate, the cutting-points bearing at
about the center of their lower edge a blunt spur, which is a modified
form of the bifurcation of the marginal teeth often found in Limax.
The marginal teeth have the usual characteristic arrangement in oblique
rows, and the separate teeth, as they pass outward, have at first the
usual rapid increase for a short distance, and thence gradual decrease
in size.
A reference to the exhaustive article on the lingual dentition of
American Fulmonata^ published in the Proceedings of the Philadelphia
Academy of Natural Sciences, April 27, 1875, by W. G. Binney, forming
part III of volume 11 of his Conchological Contributions, will show (pages
172-177) that this species differs in its dentition from all the Limaces
now known to inhabit North America. L. flavus and maximus have no
cutting-points to the sicle-cusps of centrals and laterals. L. Hewstoni has
well- developed inner cutting- pom ts to its inner lateral teeth, which in-
deed are scarcely distinguishable from the centrals. X. agrestia has also
a peculiar inner cutting-point to its laterals. L. campestris has the same
type of central and lateral teeth as the species under consideration, but
its inner marginals are simple, not bifid. L, Weinlanidi^ known only by
its dentition, no description of its external characters or genitalia having
been published (see Hynemann, Malak. Blatt., X, 212, pi. ii, fig. 1),
differs from tliis species by having all its marginals simple.
The above comparison of the dentition is given in detail, because it
is on its lingual membrane that I am forced to rely for decided specific
characters, the external characters of the animal being of little value
in alcoholic specimens.
In the genital system, there are no accessory organs. The penis-sac
is as long as the vagina, with a constriction near its commencement,
and tai)ers above to a point, below which it receives the vas deferens.
The genital bladder is oval, with a very short duct entering the vagina
above the penis-sac.
Gamp 9 : Hot Sulphur Springs 1 specimen.
My notes taken on the spot were lost. The external characters of the
animal in alcohol are unreliable : hence the brief description.
In Mr. Binney's *' Notes'' (vol. II, part III, 163), this slug was cata-
logued; among the Terrestrial Mollusks of the United States, under the
name of Limax Ingersolli^ and on pages 174 and 176 of the same work,
where the circumstances of its discovery are mentioned, it was referred
to as undescribed. In vol. II, part IV, of the same series (now in
press), it was described as L, montannt^ Ingersolt, but the necessity of
discarding the former name was not discovered by Mr. Binney in time
to make a corresponding change in the designation of the figures, which
will bear the name Limax IngersoUi^ the plates having already been
made.
396 GEOLOGICAL SURVEY OP THE TERRITORIES.
Limaz caBtaneus, sp. noy.
Smnll and slender; length less than one inch; color a lively broitn^ tcitk
a darker spot over the shield; heady tentacles^ and eye-stalks black; hottom
of foot white.
^5lf
LiDgnal deDtition of Limax ca»taneiu.
Jaw as asaal ; lingual dentition as in the other form, bat differing in
having only 34-1-34 teeth, with 12 perfect laterals. This important
difference is such as to warrant the belief that the forni may prove a
distinct species. Genitalia not examinued.
Camp 10-11: Blue River Valley ' 5specimeu8.
The above Limaces were submitted to Mr. W. G. Binney for anatomi-
cal examination. The drawings and descriptions of the jaw, lingnal
apparatus, and genitalia of both reproduced in the figures were fur-
nished by him, to whom really belongs the credit of discriminating their
specific distinction.
Limax campestris^ Binney. — ^Truckee, Nevada, 5,866 feet {Cooper)^ is
the only other mention I can find of the occurrence of this family in the
central ba^sin ; United States except Pacific slope.
HELIGIN^.
Patnla Cooperi, W. G. Binney.
Gamp 9 : Hot Sulphur Springs, Middle Park 7 specimens.
Gamp 11 : Blue River Valley 30 specimens.
Lakes, San Luis Valley 2 specimens.
Northeastern Colorado (Barber) 100 specimens.
California to Nebraska; Montana to Arizona. Most of the many
recorded localities are in the mountains; the highest being 5,500 feet
This well-known HeliXj the largest of any collected, was not uncom-
mon in Middle Park and North Park, where great numbers of dead
shells would be found in isolated spots; only a few live ones being found
in wet places in the vicinity. In the Blue River Valley, crossed a belt
a hundred yards or so wide, and apparently miles in length, where the
surface was thickly strewn with bleached shells, as though an army of
these mollusks had been overtaken on the march by universal destrnc-
tion. There was a very perceptible difference between such specimens
as were found in shaded, humid places and those living in open and drier
iHOEssoLL.] ZOOLOGY — ^HELICIN^. 397
places, in that the latter had a paler, more bleached appearance, and a
thicker shell.
Patula solitariaj Say. — CcBur d'Al^ne Mountains, 2,500 feet (Cooper ;
Hemphill.) Mississippi Valley.
Patula strigosay Goald. — Western New Mexico to the Big Horn Mount-
ains of Nebraska [Binney and Bland):, Montana to Arizona {Cooper),
Patula Hemphilli, Newc. — White Pine, Nevada, 8,000 feet {Hemphill).
Patula idahoensis, Newc. — Between Idaho City and Coeur d'AI^ne
Mountains {Hemphill).
Patula Haydeni^ Oabb. — Weber Canon, Utah {F. V. Hayden), Sub-
fossil only.
The above-mentioned species of Patula^ viz : Cooperi, solitaria, strigosa^
Meniphilli^ idahofnsis and Haydeni, are remarkably connected in form.
^^ Patula Haydeni, which may be considered as extinct, is distinguished
by its carina and equally ^ prominent, elevated, revolving ribs.' It is
allied to P. strigoaa^ and more especially to the carinated lorm described
as P. Hemphilii. The uon-carinated P. strigosa is variable, sometimes
difficult to be distinguished from depressed varieties of P. Cooperi, The
rather strongly-ribbed variety of the latter, from Bear liiver, Utah,
connects P. idahoenms with this group. In some specimens of that
species, the obsolete carina may be observed on the periphery between
the strongly-elevated oblique (not revolving) ribs. The more globose
forms of P. Cooperi may be compared with P. solitaria. In the group
of species of Patula referred to, the alliances, indicated however by
the shells alone, are associated witb well-marked specific differences in
the genitalia; in other groups, ife«o(7on, for instance, in the dentition.
Mr. W. G. Binney has lately ' directed attention to this interesting
point."— Thos. Bland, letter of March 16, 1875.
Patula Horniiy Gabb. — Fort Grant, Arizona {Horn),
Fatola Cronkhitei, Newcomb.
Gamp 9 : Hot Springs 14 specimens.
Camp 1 1 : Blue River Valley - . . 20 specimens.
Gamp F : Rio La Plata 15 specimens.
Recorded from Klamath Valley, Oregon {Oabh); White Pine Mount-
ains, Nevada, and Northern Utah {Hemphill).
Patula striatella, Anthony.
Camp 9: Hot Springs 20 specimens.
Cainp 19: Saguache 5 specimens.
Camp 24 : Clear Creek 20 specimens.
Nof th Park {Barber) 5 specimens.
Montana! {Cooper); Hell-Gate River, Montana {Binney And Blund)]
Estes Park, Colorado {Carpenter), Eastern United States.
Helix (Miorophysa) IngersoUi, Bland. Ann. N. Y. Lye. N. JET, vol. XJ,
151 ) June, 1875.
^^ Shell umhilicatedy discoidal, thin^ traTisltLcidy nearly smooth^ white;
spire Jlat^ summit subimmersed; suture impressed; whorls 5^, rather con-
veXy slowly increasing^ the last not descending, more convex below the periph-
ery ; breadth of umbilicus nearly one mill,; aperture subverticali higlier
398 GEOLOGICAL SURVEY OP THE TERRITORIES.
than broad J lunate; peristome simple^ aeute^ margins remote^ columeUar
margin slightly reflexedj basal margin subsinuate. Greater diameter 4 milL^
height 2^ miU^
Gamp 26: Baker's Park 25 specimens.
Camp 26 : CiiDuiDgham Gulch, 11,000 feet 6 8i)ecimeos.
Gamp D : Animas Valley 25 specimens*
North Park (Barber) • 10 specimens.
This beautifal little shell, described by Mr. Thomas Bland, from my
specimens, as above, was not foand by me north of the crests of the sier-
ras about Baker's Park, but was not uncommon on their southern slopes,
where I first found it clinging to vertical and all but inaccessible
cliffs in Gunningham Gulch, at an altitude of over 11,000 feet, exposed
to daily snowstorms ; yet these specimens were, if anything, finer than
those subsequently found along the Bio Las Animas. Mr. Barber's ex-
amples are all dead shells, and are not so large or perfect. They were
found at an altitude not exceeding 8,000 feet, but the station is not
stated.
Mr. W. G. Binney, who dissected the animal of this species, which
seemed with difficulty to wholly retreat into the shell, cotnmunicated
the following particulars of its anatomy :
^' Jaw low, wide, slightly arcuate, ends slightly attenuated, whole
interior surface with about 22 broad, flat, slightly-separated ribs,
whose ends denticulate either margin. This form of jaw is usual among
the Helicinae. It is of the same type as H. Lansingi (Ann. Lye N. II. of
N. Y., xi, 74, fig. 2). Lingual membrane long and narrow. Teeth abont
16-1-16. Gentrals as usual in the Relicinw ; the side-cusps and cut-
ting-points are well developed, the base of attachment longer than wide.
Laterals of same type, but unsymmetrical, and consequently only
bicuspid. The change from laterals to marginals is very gradual, there
being no splitting of the inner cutting-point. Marginals low, wide, with
one inner, long, blunt cutting-point, and one outer small, blunt cutciog-
point."
Helix lineatUB, Say.
Gamp D : Animas Valley 1 specimen.
Bio Ghama, N. Mex. (Binney and Bland)] Salmon Biver, Idaho (Hemf-
hill). North America except Pacific coast.
Helix Polygyrellaj Bid. and J. O. Gp. — Gommon on Goeur d'Al^ne
Mountains (Cooper).
Helix Columbiana^ Lea. — Hell-Gate Valley, Montana (Hemphill) ; Fraser
Eiver (Lord). Pacific coast.
Helix devia, Gld. — ^Intruding into Idaho (Binney) } Deer Lodge Valley,
Montana (Hemphill). Pacific coast.
Helix loricata^ Gld. — Sierra Nevada (Cooper). Pacific coast
Ui^MtMuLL.] ZOOLOGY — SDCININ^. 399
ETelix MuUani^ Bid. aud J. G. Gp. — C<Bur d'Alfine mi88ioD, Bitter
Root Mouutains and Kiver, Idaho {Cooper) y Idaho {Binney),
JSelix fidelis^ Gray. — Large but very pale variety, Suniass Prairie,
Fraser River (Lord). Pacific coast.
JETelix TotcnsendianajhesL — "Both slopes of the Bitter Root Mountains,
from 2,200 to 5,000 feet high. Large variety at the base of the range
to 4,800 feet; small variety in dry prairie at junction of Hell-Gate and
Bitter Root Rivers'' (Cooper). Sutnass Prairie, Fraser River; small
variety Fort Colville, summit of Rocky Mountains {Lord) ; east of Fort
Colville, Washington Territory {N. W. Bound. Surv.). Pacific coast.
The small variety from northwest Idaho has been described as a new
species by Mr. A. D. Brown under the name of Helix ptychophora (Jour-
nal de Conchologie, 1870), giving as its habitat Bitter Root Mouutains
and Nebraska. . It is regarded as a variety only.
Helix pulchella, Muller.
Gamp 11 : Blue River Valley 16 specimens.
Gamp 20 : West of Saguache 4 speciuiens.
Gamp 21 : Los Pinos Indian Agency 65 specimei s.
Gamp 26 : Howard ville. Baker's Park 50 specimens.
Gamp F : Rio La Plata 10 specimens.
North Park {Barber) 25 specimens.
**This American form {minuta) of the Old-World pulchellaj Mlill., has
only lately been found west of the Rocky Mountains. I obtained an
immature specimen near Truckee, in May. • • • Mr. Harford after-
ward found it common near Donner Luke, a few miles above Truckee ;
and Mr. Hemphill has also found them common near White Pine Mount-
ains. Not having been found north of Canada, its circumpolar distri-
bution, though asserted by Middendorf, is doubtful; he, like most
authors, considering it identical with pulckella,^ — Dr. J. G. Cooper.
Helix Dupetit-Thouarsij Desh. — Klamath Lake, Oregon (Neicberry)^
Snmass Prairie (Lor(7). Pacific coast.
Helix tudiculatay Binn. — Truckee, Nevada {Carlton). Pacific coast
SUCININ-ffi.
Buccinea Nnttalliana, . Lea.
Camp 9 : Hot Sulphur Springs 30 specimens.
Camp D : Animas Valley 1 specimen.
Warm Springs, near Salt Lake, Utah {Reid) i Snake River {Nnttall) ;
Wright's Lake and Rhett's Lake, northeast California {Newberry). Pa-
cific coast.
Sucoinea ovalis, Gould.
Camp 10 : Mouth of Blue River 1 specimen.
Eastern States.
Suooinea nuticaiia, Oouli).
Camp 9 : Hot Sulphur Springs i 12 specimens.
Bumass Prairie, Fraser River {Lord) ; Rocky Mountains of Bitter Root
Valley, 2,600 to 4,500 feet {Cooper) ; White Pine region, Nevada {Hemp-
Mil). Pacific coast.
The-se three species are hardly to be distinguished. I separated
them as above after examination of shells in the Museum of Comparative
Zoology, but they merge into one another indeterminately.
400 GEOLOGICAL SURVEY OF THE TERRITORIES.
Succinea HatcJdnsiiy Baird. — East of Fort Colville, Washington Terri-
tory (N, W. Bound. Survey) ; Lake Osojoos {Lord) ; British Colanibia.
Succinea Sillimanij Bland. — Humboldt Lake, Nevada (iSt'/Zifiian). Pa-
cific slope.
Succinea lineata, W. G. Binney.
Camp 20 : 20 miles west of Saguache 8 specimens.
Camp I) : Animas Valley 50 speciaieot».
Lakes, San Luis Valley 10 specimens.
Bank of Bear Eiver (Barber) 1 specimen.
Northeast California to Nebraska and British Columbia (Cooper);
Utah, Yellowstone River (Smithsonian Catalogue) ; Little Colorado, Ari-
zona (Palmer) ; Este's Park, Colorado (Carpenter).
I should not quarrel with any one who should prononnce some of the
smaller of my specimens to be 8. Stretchiana^ Bid. Yet, upon compari-
son with shells in the Museum of Comparative Zoology, I prefer to call
them all by the above name. They include but four living snails among
the whole number, the rest being dead shelhj. Mr. Barber's example is
a fine one.
Succinea Stretchiana^ Bland. — Little Valley, Washoe County, Nevada
( Stretch) . Pacific slope.
Succinea avara^ White Pine, Nevada (Binney). Eastern North Amer-
ica.
If, as is indicated by the map appended to Mr. Binney's catalogae
(Bull. M. C. Z., Ill, IX), the Central Province includes the valley of the
Yellowstone as far east as its mouth, Succinea Haydenij W. G. Binn.,
and S. retusaj Lea, must be considered to belong to our list, atid several
localities on the Yellowstone Eiver can be added to the distribution of
S. lineata J as well as to that of several moUusks in other families.
PHYSIDiE.
Fhysa heterostropha, Say.
Camp 9 : Hot Sulphur Springs » '. • 100 specimens.
Camp 18 : Springs east of Saguache 40 specimens.
Between the Animas and La Plata 5 st)ecimen8.
Its range from the Atlantic to the Pacific is well assured, it having
been collected in nearly every State and Territory. These specimens
show the greatest variation in [mint of size, shape, and color; yet>,inthe
absence of other types, all seem referable to this species. The Grand
River, which fiows through Middle Park, contains no Physw (or other
mollusks) tbat I could discover ; but at the Hot Springs, in a little la-
goon filled at high water, large, clear, ampuUaceaWke shells were com-
mon. In the few yards of exposed outlet of the springs of hot sulphur-
water from which the locality derives its name and celebrity, there oc-
curred in the greatest profusion a blackish globose variety about one-
fifth of an inch long. The temperature of this water was at some points
as high as 100^ F. In the basin of a still hotter spring close by, whose
waters were saturated with chlorides of sodium and magnesium, hun-
dreds of still smaller Physw (see below) were floating about in mats,
glued together by a tangle of confervoid vegetal ion and the depositions
of the water. All of these seemed to have lost the apex of the spire by
iKGBRfiOLL.] ZOOLOGY — ^PHYSID^. 401
erosioD, " which is extremely liable to happen to shells living in water
charged with alkaline salts other than lime." Yet quite as small and
bla<:k were the examples from the cold, clear, abundant springs near
Sap:uache, where there was seemingly nothing whatever to stunt their
growth.
Pliysa Wolfiana, Lea.
In the Proceedings of the Philadelphia Academy for 1869, Mr. Isaac
Lea described a species of Physa from ''the Hot Sulphur Springs, Colo-
ratio," collected by Prof. J. VV. Powell, which he named PhysaWolJiana.
Inasmuch as my shells came from the exact and very limited station and
locality (vide Observations, XIII, G7; PI. xxi, flg. 20) as his types, I
Buppose I must have it; but as I cannot separate to my satisfaction
those which resemble that shell as described and figured, from those
which do not resemble it, I have remanded all to the foregoing species.
Phym Lordij Baird. — British Columbia (Lord), replacing P. hetero-
strophaou the higher ground toward the Rocky Mountains ; east of Fort
Colville, Washington Territory (Northwestern Boundary Survey). It is
not unlikely that P. ClarJcei and the two following species will prove
identical with this, diifering only in size and color. Here, as in Limnea,
the shell is subject to such variation that it is precarious to predicate
specific rank upon the shell alone, particularly it' the specimens be few
and localities isolated.
Physa ampullaceajGonld, — Oregon and Washington Territory (Cooper);
Bhett's Lake, Caliioruia, and Upj)er Kiamath LuUe, Oregon (Newberry).
Pkysa ancillaria^ Say. — Ruby Valley, Nevada (Simpson),
Physa gyrina, S'dy. — Carson, "S ewadd (Wheatley)', Nevada (Simpson).
Missouri River.
Physa humerosa^ Gould. — Colorado Desert, Pecos River (Blalce).
Physa Orosvenorii, Lea. — Dayton, Nevada ( Wheatley).
Physa parva, Lea. — Little Valley, Nevada ( Wheatley).
Physa Hawnii, Lea. — White Pine, Nevada (IlemphUl).
Physa Saffordii, Lea. — Fort Hall, Idaho, and Snake River Valley,
Utah (Reid); Nevada an<l Eastern Idaho (Hemphill).
Physa virgata. — Gila River ( Gould). Southern California.
Physa propinqua, Tryon. — White Pine, Nevada (Hemphill)] Jordan
Creek, southwest Idaho (Oabb).
Physa occidentaliSj Tryon. — Fort Colville, Washington Territory (Horn) ;
Warners Valley, Oregon (Oabb) ; Truckee, Nevada (Carlton).
Physa Blandiiy Tryon. — Truckee, Nevada (Carlton).
Physa malleata, Tryon. — Hell-Gate River, Montana, and Fandango
Valley, a part of Goose Lake Valley, Oregon (Oabb).
Physa Nnttallii, Lea. — Lewis River, Idaho (Nuttall).
Physa Cooperi, Teton.
Between the Animas and La Plata 5 specimens.
Also recorded from a spring in Crane Lake Valley, northeast Cal-
ifornia (Oabb). I do not feel quite sure of this determination, because
of the immaturity of the specimens, and the fact that I do not have
access to types ; nor do I altogether trust in the validity of the species.
Bnlinns hypnomin, Linn^us.
Camp 9-10 : Grand River Valley 50 specimens.
Bear River (Barber) * 5 specimens.
26 H
402 GEOLOGICAL SURVEY OP THE TERRITORIES.
Recorded also from Hell-Gate River, Montana {Cooper) ; Utah ; Ma-
lade River, Idaho {Hemphill)] Washington Territory; Yellowstone
River (timitJisonian Catalogue) ^ British possessions (l/or<2) northward
Cosmopolitan.
PLANOEBIN-ffi:.
Helisoma plexata, sp. NOV.
Shell a little larger than P. Trivolvis, Say, of irregular proportions^
fragile] whorls 4-5, the inner ^-^ of the spire angulated and coiled in a
plane, tchich is considerably iiiclined to the plane of the outer revolution in
such a tcaii that the carina of the third whorl rises into a sharp shoulder on
the right side, and on the lift side sinks underneath the overfiotcing last ichorlj
which takes on a sudden increase in old. age. A similar, but less, change in
the plane often occurs again in the fourth whorl, giving a very twisted ap-
pearance to the shell. Surface marked by irregularly -crowded, tcavy, raised
lines of growth. Umbilicus broad, exhibiting the tcell-rounded whorls to
the apex. Aperture somewhat oblique, pretty regularly pyriform in outline,
the vertical slightly exceeding the horizontal diameter, and embracing a con-
siderable portion of the body whorl, well to one side of the median line.
Peristome gently reflected, slightly thickened within, and fully lined with
an opaque white deposit, which also forms a thick and welldefined callous
connecting the ends. Color yellowish horn to reddish-broicn {becoming
almost black behind the aperture), most specimens abundantly banded and
streaked with revolving lines of ochraceous red, and fine black threads.
spire. Aperture. Section at apertnra
RhowinK cbanpe
of plaue in revola-
tion.
Sjiint Mary's Lake, Antelope Park 25 specimens.
This species existed in countless numbers in the above-mentioned
lake, which is a small sheet of water held among precipitous cliflPs,
that afford it no visible outlet. It seems to be merely a " sink " for
the melted snow of the snrrounding heights. All of the hundreds of
individuals seen, possessed, in a more or less marked degree, the
twisted appearance, resulting from the change of plane in the old age
of tbe shell, which is their most striking character. How the species
came, almost entirely alone, to inhabit this secluded lake is a problem,
complicated by the fact that there probably is not another larg;e Plan-
orbis within iifty miles. That the wild fowl, abundant on the lake,
brought the eggs clinging to their feet, may be a plausible explanation;
but where did they bring them from, and when f The bottom of the
lake is, for the most part, rough conglomerate rock, and it is in many
places filled with heavy water-plants, which may account lor the pecu-
liarities of the shell.
The members of the family Planorbidce, seem to be particularly sub-
ject to sudden and eccentric deviations from the normal form of the
group. Many curious examples have been noticed. The genus Valtaia
seems also subject to similar deformities, which Prof. Alpheus H^att, of
Cambridge, Mass., has been paying special attention to of late, in the
DfGBRfiOLL.] ZOOLOGY — ^PLANORBIN^. 403
conrse of some paleootological investigatioDS. GoncerDiDg this matter
Professor Hyatt writes as follows, in a letter dated February 10, 1876:
"These variations have been studied only with reference to the shell,
bat the changes of form are so great in this external organ, that one
naturally infers corresponding ditferences in the animals themselves.
The principal papers heretofore published upon these interesting shells
are but two in number: one by Hilgendorf, in the Monatsber. d. kongl.
Preuss. Akad. d. Wissen., 1866, upon the fossil forms of Flanorbis mul-
tiformis; and one by M. Pir6, upon Flanorbis complanatusj in the Annales
de la Soc. Malacol. de Belgique for 1871. The recorded information is
therefore scanty, and it would be a very important service to conchology
and paleontology if every one who has met with abnormal or distorted
forms, in the course of his collecting of land or fresh-water shells, would
make public all the information he has in connection with those discov-
eries. Records of such experiences are extremely desirable.
" Both of the papers alluded to above are accompanied by figures, and
show a very remarkable series of forms, which vary from the flat spire
with equal umbilici, to those which are completely trochiform, and fron
these to specimens entirely unwound, like a wire corkscrew. I have
myself studied attentively the Steinheim beds described by Hilgendorf,
and can confirm his results so far ds the extreme variations of form are
concerned, though in other respects his paper is full of erroneous state-
ments, especially with regard to the genetic connections and stratigraph-
leal distribution of the varieties.
" I have also a very remarkable series of shells, probably belonging to
Valvata, which I owe to the kindness of Prof. Edward S. Morse. They
were collected by Prof. C. F. Hartt in marl laid dry by the drainage of
Lawlor's Lake in Nova Scotia. These are equal to any described species
in variation, some of them being actually unwound, with a perfectly
cylindrical outline, to the mouth of the shell. What the governing
peculiarities of the locality last named may have been at the time the
marl was deposited, I cannot say, but the condition of the Steinheim
Lake during the Tertiary period, and of the small ponds, described by
M. Pir6, resembles closely that of the localities described in your
paper.
*' The Steinheim Lake was evidently, as shown by Quenstedt and Fraas,
an isolated sheet of water about a mile in diameter. The ponds of
Magn^e, according to M. Pir6, are fed only by rain-water, but are never
frozen and never dry.
** Not only, therefore, is the occurrence of these extreme variations
exceptional, but they appear in localities presenting certain excep-
tional characteristics. These characteristics are well worth investigating,
since it seems as if a direct correlation existed between the extreme
variations of the shells, and some physical cause common to all tbe
Jocalities in which the distorted specimens have been found. That the
variations are not distortions in the ordinary meaning of that word, can
be readily understood by any one who has studied an extended series of
thorn. The most aberrant of these varieties in Steinheim has descendants,
which perpetuate its peculiarities for what must have been a consider-
able lapse of time, forming races of greater or less importance; and M.
Pir6 inferred the same fact at Magn6e, from dead shells found buried in
the mud at the bottom of the cisterns. I have no doubt that the reniust
be a vast array of similar experiences awaiting any explorer of the iso-
lated lakes and ponds of this country, and I hope your publication will
open the way for many similar observations. In no other direction can
we look for more light upon the mode of origin of new races and forms,
f
404 GEOLOGICAL SURVEY OP THE TEKRITORIES.
and the causes which lead to their prodnctioD, than by the study of siidi
isolated localities, where causes are reduced to their least complicated
state, and results reach their maximum, so far as the observability and
variety of the characteristics are concerned."
Helisoma trivolvis, Sat.
Pond between the Animas and La Plata ^ 10 specimens.
San Luis Lakes , 5 specim«i&
There is a long list of recorded localities from all the Territories, as
well as British America and the Pacific coast, so that it seems univer-
sally distributed over this continent.
The pond first alluded to was entirely isolated, and several acres in
extent, resorted to by vast flocks of wild fowl, and inhabited by all sorts
of fresh-water and amphibious life. The bottom was mudd^^, and nearly
the whole expanse choked with luxurious vegetation.
All of the species, which were abundant, seem to belong to this
species, although there are scarcely two alike. One resembles closely
Flanorlns macrostomusj Whiteaves; another in near P. tumens^ Cpr.; a
third variety might be identified as P. glabratus^ Say, if that shell were
dextral; yet, while all difi'er in development and in color, all agree in
being very fragile, which may be owing partly to scarcity of lime in the
water, aud partly to the soft bottom ) and in having a short vertical
diameter, which peculiarity may have been acquired by them from the
necessities of their habitat, since snails having shells with small breadth
of beam could most advantageously pass between the stalks of standing
water-plants which everywhere crowd the pond. This species is an
inhabitant of the United States generally.
Helisoma ammon, Gld. — Colorado Desert {Blake) ] Klamath Lake, Ore-
gon, and Rhett Lake, California (Neicherry) ; east of Fort Colville, Wash-
ington Territory {Northwestern Boundary Survey), Pacific slope.
Helisoma Traskeiy Lea, is probably a synonym of the above. Cali-
fornia.
Helisoma corpulenitis, Say. — Oregon and Washington Territory ( United
States Exploring Expedition) \ Lake Osoyoos, Washington Territory
(Marsh)) British Colombia (Xor(?) ; Okanigan Eiver, Washington Terri-
tory {Cooper) ; Pacific Coast and Guatemala. It seems doubtful whether
this is not a synonym of i/. trivolvis.
Planorbis oregonensis^ Try on. — Pueblo Valley, on the boundary be-
tween Oregon and Nevada, " from a thermal spring, water above blood-
heat" {Gahb).
Planorbis subcrenatus, Cpr. — Oregon {NuttalC) ; Washoe, Nevada {New-
comb); Snmass Prairie, British Columbia {Lord). California.
Planorbis Hornii^ Tryon. — Utah {8uro, W. of 100th if.); Truckee Eiver,
Nevada {Carlton).
Planorbis gracilenttis, Gld. — Colorado Desert ( Weibb). This seems to
be a northern form of P. Liebmanni. Dunker.
7 •
Oyraulus parvus, Say.
Camp 9: Hot Sulphur Springs 1 specimen.
Arkansas River, ten miles below Granite 5 specimens.
Between Bio Animas aud Bio La Plata 2 specimens.
Saint Mary's Lake, Antelope Park 60 sj)ecimen8.
North Park {Barber) , . . 6 specimens.
xKomsuLu] ZOOLOGY LIMN-EIDiE. 405
It occurs also in Hell-Gate River, MontaDa (Coop^); Ccear d'Alfine
Xake, MoQtBDa {Hemphill) ; Ruby Valley, Nevada {ISimpson) ; and aloug
the Yellowstone {Smiths. Catal.). Eastern States.
Oyratilus verniioularis^ Gld.— Truckee, Nevada, altitude 5,866 feet,
xare ; Dalles, Oi-egon {Cooper). Santa Cruz northward.
POMPHOLIGINJE.
•
Pompholyx effusa^ Lea. — ^Near White Pine, Nevada {Hemphill)] north-
eastern California {Newberry). Sacramento Valley.
• Garinifex Newberryi^ Lea. — Klamath Lake, Oregon {Newberry). Cali-
fornia.
Varticifex Tryoni^ Meek. — Fossil in Tertiaries of Nevada {King).
t Ancylus paralleluB, Haldeman.
North Park (Earner) 4 specimens.
Among the shells brought home by Mr. Barber were four apparently
full-grown specimens, and one young one, of an AncyluSy none of which
contained the animal. While closely resembling the figure of A. cau-
rinusy Cooper, given on page 144 of Part II, of Binney and Bland's
Land and Fresh- Water Shells of North America, careful comparison
vith the large series in the Museum of Comparative Zoology failed to
establish any great difference between them and A.parallelm. As,
however, this latter species has not been found hitherto, out of New
England, it seems only proper to look upon the apparent identity of
the Colorado and eastern shells, with caution. A slight difference in
the angle of the sides en profile may, perhaps, be noticeable between
them.
Ancylus Newberryij Lea. — Klamath Lake, Oregon {Newberry).
Ancylus kootaniensiSy Baird. — Rivers Kootanie and Spokane {Lard).
Ancylus patelloides, Lea. — Spokane River, Washington Territory,
[approaching A. kootaniensis] {Hemphill). California.
Acroloxus Nuttalliij Hald. — Oregon {Nuttall); lower part of Snake
River, Washington Territory {Hemphill). California.
LIMN^ID^.
Lixnnea stagnalis, Linn^us.
Between the Animas and La Plata 2 specimens.
Fraser River, typical, fine, and abundant {Lord)] east of Fort Colville
{Northwest Boundary Survey) ; Rhett's Lake, California {Newberry); Ruby
Valley, Nevada, and southern Utah {Simpson). Circumpolar.
Idmnea snmassi, Baibd.
Between the Animas and La Plata 1 specimen.
Bast of Fort Colville, Washington Territory {Northwest Boundary
Survey); Su mass Prairie (Xord).
Limnea Haydenij W. G. B. — Yellowstone and Big Sioux Rivers {Hay-
den); Ruby Valley, Nevada {Simpson).
Limnea — ?
Camp 30 : Rio Grande, above del Norte 60 specimens.
Bemauks. — "Near L. Bowelliiy Try on.'' — Dr. Jas. Lewis, in letter.
406 GEOLOGICAL SURVEY OF TUE TERRITORIES.
Limnea palnstris, Muller.
Between the Animas and La Plata 2 specimeDS.
Co\umbm River {Niittall); Klamath Lake and Sumner Lake, Oregon;
Ehett's Lake and Wright's Lake, California {Neicberry); Hell-Gate
Elver and Missouri Elver above Falls {Cooper). Circuropolar.
Limnea Ifnttalliana, Lea.
Between Animas and La Plata Elvers 75 specimens.
Eemarks. — Often considered a synonym of L.palustriSj with which,
in the West, it seems to be co-extensive.
Limnea desidiosa, Say.
Gamp 9: Hot Sulphur Springs 10 specimens.
CamplI: Blue River Valley.. 10 sijecimens.
Lake Osoyoos, Washington Territory (Lord)} Missouri Eiver above
the Falls [Cooper) ; Yellowstone Eiver (Hayden). Eastern United States
and Mississippi Valley. This shell is called Limnea obrussa in many
western lists.
Limnea catascopium^ Say. — New Eugland to Lewis [Snake] Eiver, and
through British America (Binney) ; Lake Utah {Burton) ; Idaho (?).
Limnea Binneyi, Tryon. — Hell Gate Eiver, Montana (Binney).
Limnea emarginata^ Say. — New England to Washington Territory
[Auct).
Limnea bulimoidesj Lea. — Oregon {NuttaJl ; Hayden).
Limnea Traski, Tryon.
Golorado 6 specimens.
A Galifornian species..
Limnea hnmilis, Say.
Gamp 17 : San Luis Valley 2 specimens.
Gam p 26 : Ho ward ville. Baker's Park 1 specimen.
Hell-Gate Eiver, Montana {Cooper). All over the continent
IL^jnneafermginea, Haldeman.
Between the Animas and La Plata 2 specimens.
Oregon (Nuttall). " If not L. ferrugineaj it may be new.''— Dr. Jas.
Lewis, in letter.
Class CONCHIFERA.
Order DIMYARIA.
GOEBIGULAD^.
Sphcerium atriatinum^ Lamarck. — Hell Gate Eiver and Missouri Biver
above the Falls (Cooper) '^ Humboldt Eiver, Nevada {Hepburn). East-
ern North America.
Sphcerium occidentaU, Prime. — Hell-Gate Eiver (Cooper). Northern
States and Gauada.
Sphcerium dentatum^ Hald. — Oregon {21'uttall).
isGBBUOLL.] ZOOLOGY UNIONIDiE ^LIST OP AUTHORITIES. 407
Sphcerium patellaj Gonld.— Walla- Walla, Oregon (J7. S. Uxpl. Exped.).
Sphccrium lenticula^ GId. — Lake Tahoe, Klauiatb aud Carsou EiverK,
Cal. {Cooper).
Sphagnum tumidumj Baird. — Sumass Prairie, Fraser Kiver (Lord).
Sphccrium spokanij Baird.— ^Spokane and Kootauie liivers {Lord;
Hernphill).
Sphccrium tenue, Prime. — I am confident that I secured this species
(one specimen) at tbe liio La Plata. It has been recorded, I think,
from Montana and anotber northern locality. It is$ a boreal species.
Fisidium abditam, Haldeman.
CampO: Hot Springs 30 specimens.
Camp D : Animas Valley 1 specimen.
Saint Mary's Lake, Antelope Park 1 specimen.
Raft River, near Fort Hall, Iduho {Reia); Truckee River {Carlton),
All over tbe continent.
My specimens vary greatly in color, but seem to be all referable to
this widely-distributed species. Many are about half-grown.
Pisidium compressum^ Prime. — White Pine, Nevada ; Owen's River,
California (Hemphill)^ Northern States and Canada.
Pisidium occidentale^ Newc. — Truckee River, Nevada {Carlton). Cali-
fornia.
Pinidium ultramontanum^ Prime. — Canoe Creek, Pitt River, California
(Cooper). '
UNIONID^.
Unio luteolwt. Lam. — Missoui i River, above the Falls {Cooper). United
States generally.
Margaritaiia margaritifera^ Linn. — Missouri River above the Falls;
Spokane River below Coeur d'Alene Lake {Cooper)] Salt Lake, Utah,
or Fort Hall, Idaho {Rtid) ; Truckee River, Nevada ( Carlton). Cosmo-
politan. This Mollusk is eaten by tbe Indians east of the Cascade
Mountains.
Anodonta angulata^ Iteti, — Idaho, Montana {Cooper)] Columbia Jliver
{Lord.) Considered at most only a variety of the foregoing.
Anodonia oregonenniH^ Lea. — Abundant east and west of the Cascades
{Lord) ] Montana ( Cooper).
Anodonta Nuttalliana^ Lea. — Idaho {Cooper).
Anodonta whalamatemis^ Lea. — Idaho, to British Columbia {Cooper).
LIST OF AUTHORITIES.
The following list of authors is intended to include all of the books
and papers ])ublished in English tbat contain direct reference to the
mollusca of the Central Province, so called.
Such general works as Gould's Shells ol' the United States Exploring
Expedition, Dr. Binney's Terrestrial Mollusks, Haldeman's Monograph
of the Limuoiida), Lea's Observations, Binnev and Bland's Land and
Freshwater Shells of North America, and Pfeifter's Monographia
Heiiceorum, must, of course, be consulted in working up the *jio11u8c<iq
fauna of any district, but scarcely requii>3 mention among special author-
ities.
Baird. Descriptions of some new species of shells collected in Van-
couver's Island and in British Columbia, by J. K. Lord, 1838-02 :
by Wm. Baird, M. D. Proc. Zool. Soc. of Loudon, 1803-07.
408 GEOLOGICAL SURVEY OF THE TEBRITOKIES.
Bland. Notes on the sub-generic characters oi Helix JamaicensiSy GbemD.,
and on certain terrestrial mollusks from Haiti, with descrlptioD
of a new species of Helix from Colorado : by Thomas Bland.
Ann. N. Y. Lye. N. H., Xf, 146.
Bland and Binney. On the generic position of Helix Neuberryana: by
Thos. Bland and VV. G. Binney. Am. Jour. Coucbology, Vli,
190 ; plate 17, figs. 3 and 4.
Bland and Cooper. Notice of land and fresh- water shells collected by Dr.
J. G. Cooper, in the Rocky Monutaius, etc. : by Thos. Bland.
Ann. N. Y. Lye. N. H., 1801, 362.
Binney. Report on the land shells collected on the survey: by W. G.
Binney. In the reports of explorations and surveys for a rail-
road from the Mississippi River to the Pacific Ocean, etc,
VI, IIL
Descriptions of American land shells : by W. G. Binney. Proc
Phil. Acad. Sc, IX, 18.
Notes on American land shells. No. 3: by W. G. Binney. Proc
Piiil. Acad. Sc, X, 197.
A supplement to Amos Binney's Terrestrial MoUusks of the
United States, constituting volume IV of the same: by W. G.
Binney. Boston, 1859. [From the Journal of the Boston Soc
of Nat. Hist.]
Catalogue of tne terrestrial air-breathing mollnsks of the United
States: by W. G. Binney. Bull. Mus. Comp. Zool., Ill, ix.
Notes on American land shells and other miscellaneous coucho-
logical contributions: by W. G. Binney. Proc. Phil. Acad.
Sc, 1874 and 1875. [Also bound up in two volumes for the
author, at Burlington, N. J. I
Carpenter. The moUusks of western North America: by P. P. Cabpen-
TEB. Washington, Smithsonian Institution, 1872. [Reprinted
from Keport to the Brit. Assoc, etc|
Carlton. List of the shells of Truckee River and vicinity: by H. P.
Carlton. Proc Cal. Acad. Sc, IV, 57.
Confad. Description of a new species of Melania : by T. A. Coxead.
Proc Phil. Acad. Sc, Vll, 269.
Cooper. List of shells collected by Mr. Schoolcraft in the western and
northwestern terniory : by Wm. Cooper. In the appendix to
Narrative of an expedition through the Upper Missouri, etc.,
under the direction of Henry B. Schoolcraft. New York, 1834.
Report on the niollusca of the survey : by Wm. Cooper. In the
Pacific Railroad Reports, XII, pt. ii. [Same as afterward ap-
peared in Cooper and Suckley's Natural HiiJtory of Wsishington
Territory : New York, 1859.]
Croper. Geographical catalogue of the mollusca found west of the Rocky
Mountains, between latitude 33^ and 49^ north: by J. 6.
Cooper, M. D. In connection with geological survey of Cali-
fornia. San Francisco, 1867.
On the distribution and localities of west coast helicoid land-
shells: by J. G. Cooper, M. D. Am. Jour. Conchology, IV,
211.
West coast helicoid land-shells : by J. G. Cooper, M. D. Proc
Cal. Acad. Sc, III, 331.
"West coast fresh-water univalves. No. 1 : by J. G. Cooper, M.
D. Proc Cal. Acad. Sc, IV. 92.
Notes on west coast land-shells. No. 2: by J. G. Cooper, M. D.
Am. Jour. Conchology, V, 199.
IKOBB80LL.] ZOOLOGY — LIBT OP AUTHORITIES. 409
On shells of the west slope of North America: by J. G. Cooper,
M. D. Proc. Cal. Acad. Sc, IV, 160.
No. 2 of same. Ibid., 171.
On new California Tnlmonata, etc: by J. G. Cooper, M. D.
Pror^. Phil. Acad. Sc, 1872, 143.
I>all. On a species of Helix from California, supposed to be new : by W.
H. Dall. Am. Jour. Conchology, II, 328.
On a new subfamily of fiuviatile mollusca: by W. H. DAX.L,
Prpc Cal. Acad. Sc, III, 204.
On the genus PompJiolyx and its allies, with a revision of the
LimnsBidsb of authors : by W. H. Dall. Ann. N. Y. Lye N.
M., IX., 33o.
Gabb. Descriptions of three new species of land-shells from Arizona: by
Wm. M. Gabb. Am. Jour. Conchology, II, 330.
Description of a new Helix from Utah : by Wm. M. Gabb. Am.
Jour. Conchology, V, 24.
Gould. Catalogue of shells collected in California by W. P. Blake, with
descriptions of the new species : by Augustus A. Gould, M.
D. In appendix to the preliminary geological report of Wm.
P. Blake to Lient. R. I. Williamson. Washington, 1855.
Descriptions of new species of land and fresh-water shells from
western North America : by A. A. Gould. Proc Bost. Soc
N. H., V, 127.
Lea. Description of new fresh-water and land-shells; by Isaao Lea.
Trans. Am. Philos. Soc, VI. [Incorporated in Observations on
the genus UniOj etc., II.]
Continnation of paper on fresh-water and land shells : by ISAAO
Lea. Trans. Am. Philos. Soc, IX, [Incorporated into Obser-
vations,' etc., IV.]
Descriptions of new freshwater shells from California : by Isaao
Lea. Proc Phil. Acad. Sc, VIII, 80.
Descriptions of a Helix and two new Planorbes: by ISAAO Lea.
Proc Phil. Acad. Sc, X, 41.
Descriptions of six new species of Succinea from the United
States : by Isaao Lea. Proc Phil. Acad. Sc 18C4, 109.
Descriptions of twenty -four new species of Physa of the United
States and Canada: by Isaao Lea. Proc Phil. Acad. Sc
18C4, 114.
Descriptions of six new species of fresh-water shells : by Isaao
Lea. Proc Phil. Acad. Sc, 1809-70, 124.
Lord. The naturalist in Vancouver's Island and British Columbia: by
John Keast Lord, naturalist to the British northwestern
boundary commission. 2 vols. London, 1866.
ffewcomb. Catalogue of Helices inhabiting the west coast of North
America, etc : by Wesley Newcomb, M. D. Am. Jour. Con-
chology, I, 342.
Addition to catalogue of Helices, etc., ibid., II, 13.
Desciiption of new species of land shells: by W. Newcomb, M.
D. Proc Cal. Acad. Sc, III, 179. •
Description of a new American species of Helix: by W. New-
comb, M..D. Am. Jour. Conchology, II, 1.
,^ Description of a new American Helix: by W. Newcomb, M. D,
Am. Jour. Conchology, V, 165.
Prime. Monograph of North American Corbiculadse : by Temple
Peime. Washington, Smithsonian Institution, 1865.
410
GEOLOGICAL SUEVEY OF THE TEkEITORIES.
Stearns. Eemarks on fossil shells in the Colorado Desert: by £. C.
Stearns. Proc. Cal. Acad. Sc, IV, 229.
Stimpson. Researches ou the H> drobiioa) and allied forms : by Dr. Wm.
Stimpson. Washiugtou, Smithsonian institution, 1865.
Tryon. Catalo^^ue of the species of Physa inhabiting the United States :
by George W. Tryon. Am. Jour. Gonchology, I, 165,
^^Descriptions of new species of Amnicola^ Pomatiopsis, Sonutto-
gyrusy OabbiUy Hydrobia^ and Rissoa : by George W. Tryo».
Am. Jour. Gonchology, I, 219:
Descriptions of new species of North American Limnssidae : by
George W. Tryon. Am. Jour. Gonchology, I, 223.
Review of the Goniabases of Oregon and Galifornia: by Gborgb
W. Tryon. Am. Jour. Gonchology, I, 236.
' Catalogue of the species of Limnea of the United States : by
George W. Tryon. Am. Jour. Gonchology, I, 247.
New localities for Physce: by George VV. Tryon. Am. Jour.
Gonchology, II, 7.
Monograph of the family Strepomatidse : by George W. Tbyok.
Am. Jour. Gonchology, I and II.
TOPOGRAPHY AND GEOGRAPHY.
IlEI>OIlT8
OF
HENRY GANNETT, S. B. LADD, AND A. D. WILSON.
411
i
4.
GEOGRAPHICAL REPORT OF HENRY GANNETT, M, E., TOPOG-
RAPHER DIRECTING MIDDLE DIVISION.
IJ^TRODUCTORY LETTER.
Sir: I have the honor to 8nbaiit to jou herewith my report on the
geographical work of the middle diviaiou of the survey during the
season of 1874.
The party in my charge was composed as follows : Dr. A. C. Peale,
geologist: Fred. D. Owen, assistant topographer; Frank Kellogg and
Arch. R. ^alloch, general assistants, with two packers and a cook.
The party left Denver on July 21, and i)roceeded to the field of work
via Fairplay, Mosquito Pass, and Tennessee Pass, returning by the
Bouthern route, via Cochetopa Pass, San Luis Valley, Poncho Pass, and
Canon City, reaching Denver November 10.
The area worked is five thousand three hundred square miles, in doing
•which eighty-six stations were occupied, or an average of one in every
8 miles.
I would here express my thanks to Mr. Q. F. Bond, Indian agent at
the Los Pinos agency, for assistance rendered by him during the season.
Very respectfully, your obedient servant,
HENRY GANNETT.
Dr. F. V. IIA.YDEN,
United States Oeologist
413
/
CHAPTER I.
The district assigned to the middle division for the field season of
1874 was bounded as follows: Commencing at the intersection of the
Orand River with the meridian of 109° 30', the north line follows the
Orand up to the mouth of the Eagle River; thence the Eagle River to
its intersection with the parallel of 39o 16' ; thence west, along this
parallel, to the meridian of 107O; south on tins meridian to the parallel
of 38° 20' ; west on this parallel to the meridian of 109° 30', and north on
this meridian to its intersection with the Grand River. The total area
of this district is seven thousand five hundred square miles. Of this
area the party in my charge has worked all of the country lying be-
tween the Grand and Gunnison Rivers, the strip lying between the
parallel of 39° 15' and the Eagle River, and a small area south of the
Gunnison River, between the one hundred and seventh and one hun-
dred and eighth meridians.
PREVIOUS EXPLOBATIONS IN THE DISTRICT UNDER CONSIDERATION.
With the exception of a little work done along the borders, this
country was as little known as any part of the Western Territories. No
map, representing even the most general features, was in existence.
In 1845, Fremont, at that time a lieutenant in the Corps of Topo-
graphical Engineers, skirted the northern border for a short distance.
He came up the Arkansas River, crossed the main divide at Tennessee
I^ass, and traveled down Eagle River as far as the mouth of/ creek.
Here he crossed the river and took the trail over to White River, which
stream he followed down some distance, then crossed the country to the
Green River, thence to Salt Lake City. He was in the country in
which I worked during last season, only while on the Eagle River for
a distance of about thirty miles.
In the autumn of 1853, Captain Gunnison, with a large force of
soldiers and civilian employes, including topographers and a geologist,
and a large wagon-train, came into this country by way of San Luis
Valley, <3ochetopa Pass, and Cochetopa Creek. From the mouth of
Cochetopa Creek his course was down the Gunnison as far as the mouth
of White Earth Creek, sixteen miles, within which distance he was
obliged to cross the river several times. At the mouth of White Eacth
Creek he was obliged to leave the Gunnison and cross the rolling,
broken country south of it, in a southwesterly direction, to Lake Fork,
which he crossed with considerable diflQculty several miles above its
mouth. He then continued down its west bank nearly to the Gunnison,
where he wound around the side of the mesa to the valley of Mountain
Creek. He traveled up the valley of this creek, in a direction nearly
415
416 GEOLOGICAL SUBVEY OF THE TERRITORIES.
south, for several miles, then left it, gaining the summit of tbe plateaa.
On this summit he traveled in a direction fjeuerally west, cros^
several streams, until he reached a branch of CeboUa Creek. He trav-
eled down' this branch and the main creek to a point only one mile
from its mouth, where. the Gunnison is in a tremendous eauon. There
he left CeboUa Creek and crossed the ridge to Cedar Ci^eek, a branch of
the Uncompahgre Kiver. Thence he followed Cedar Creek and the
Uncompahgre to the Gunnison Eiver. He forded the Gunnison at the
mouth of Koubideau's Creek. Thence his course followed a low,
trough like depression in the valley near the mouth of the Gunnison to
the Grand River, which he forded about five miles above the mouth of
the Gunnison. Below this point bis route followed the course of the
Grand quite closely tor a long distiince below what he supposed to be
the mouth of the Dolores, finally crossing to the Green, and theocre to the
Sevier, whence it goes nenrly north to Salt Lake City. The topo|2:raph-
icai work done by this expedition consists of a narrow belt on each side
of their line of travel. The general course of the Gunnison, except in
the great canon, was mapped.
A few months later, Fremont passed over the same route, on his way
to California.
In the summer and fall of 1873^ Lieutenant Ituffner, United States
Engineer Corps, had a party within this district, under the immediate
direction of civilian assistant H. G. Prout. This party surveyed tha
principal part of Ohio Creek, and the head of Anthracite Creek, a
branch of the North Fork of the Gunnison Eiver — in all, perhaps, two
hundred square miles. His map, of which this area forms but a small
portion, was published in the sjmng of 1874. In Mr. Prout^s report,
which accompanies the maps, he gives certain names to some of tbe
prominent mountain-peaks in this area. These names would be plo^ced
on our maps, were it possible to identify the peaks on which they have
been bestowed, but neither from his report nor from his map can the
names be located.
aEOGRAPHY OF THE DISTRICT.
«
In this report, I shall take up the whole country west of tbe Sawatch
range, over which I have worked during the two seasons of 1873 and
1874, in order to consider the Elk Mountains and their spurs as a whole,
even at the risk of repeating some of my report on the field-work of 1873.
West of the Great Sawatch range, the county is drained by the two
rivers, the Grand and the Gunnison. The Gunnison is the largest and
most important branch of the Grand, while the Grand, by its union with
the Green, gives rise to the Eio Colorado, which drains nearly all of the
southwestern i)art of the United States.
The principal branches of these rivers are: of the Grand, from the
south. Eagle River, Roaring Fork, Divide Creek, and Plateau Creek;
of the Gunnison River, from the north, Taylor River, Slate River, Ohio
Creek, Smith's Fork, and the ^orth Fork of theGunnison, and fi'om the
south, Texas Creek, Cochetopa Creek, Lake Fork, (or Rio delaLagana
of the Spaniards,) Cebolla Creek, and the Uncompahgre River.
The country between these two large streams, the Grand and Ganni-
son, consists, in the eastern part, of the system of mountains known as
the Elk Mountains,' with its spurs, which, at its western extremity, falls
into plateau, considerably broken down by denudation. The Elk MouDt-
aius, with their si)urs, occupy the whole area between the Eagle River
and the i)ortion of the Grand River between the mouths of the Ea^le
and Routing Fork on the north, and the Gunnison from its head to tbe
GANNETT.] OEOGBAPHY — ^ELK MOUNTAINS. 417
month of its North Fork on the south and west. The whole area covered
l3y this system is aboat three thousand two hundred square miles. This
^aitimate covers not only the high monntaiu region, but also all the spurs
directly connected with the rsiiige, thus including much rolling and val-
ley country'.
The principal part of this mountain system is in the form of a series
of parallel ranges connected transversely by low saddles, and having a
<lirection about north 30^ west and south 30^ east, or essentially the
aame direction as the Sawatch ivnd Park ranges and other ranges in
Colorado. The most important of these ranges, both in height and con-
tinuity, is the most eastern, the one which is terminated on the north by
Sopris' Peak, and includes Capitol Peak, Snowmass Mountain, Castle
l?eak, and others of the principal peaks of the system. This range joins
t he Suwatch range in a heavy, broad, and comparatively low ridge, in
latitude 38o 45'.
Farther west, the parallel ranges are not as continuous, or as high,
but all have a uniform direction, until we reach the western part of the
fi&ystem. In about the longitude of the head of Ohio Creek, i, e , longi-
t ude 107^ 6', the character of the grouping changes, and the mountains are
ill isolated groups, irregularly disposed. But here, as farther east, the
drainage still has the same direction, slightly west of north and east of
MOuth, as is the case with Ohio Creek, Anthracite Creek, and many
others, as is seen by a glance at the map.
The drainage of the Elk Mountains toward the north into the Grand
is carried entirely by Koaring Fork and its branches; to the south b^^
the Gunnison and its branches from the north above its North Fork ;
and on the west by the IS'orth Fork of the Gunnison.
Frying-Pan Creek, one of the largest branches of Bearing Fork, is
in a very narrow valley, or close caiion throughout its course, from the
Sawatch range to its month. It is bordered on each side by broad, high
ridges, reaching to the timber-line or above. The same broad, massive
character appertains to the ridges separating all the branches, which
unite to form lioaring Fork, as far around toward the west as Castle
Creek. Here we reach the principal range of the Elk Mountains, and
the character of the mountain-forms changes materially. The broad,
massive ridges give way to sharp, conical peaks, ragged, serrated
ridges, pinnacles, and spires. They increase in elevation from 11,000 or
J 2,000 feet to 13,000 or 14,000. The mountains present great diversity
of colors, some being of light-gray trachyte, others of red, maroon, and
brown sandstone.
The principal range of this mountain system separates Boaring Fork
from Bock Creek. It is a very well deiined range as far south as the
divide, and a few miles beyond. Farther south it diminishes in eleva-
tion and loses its distinctive character, in a number of spurs, separating
branches of the Gunnison. Of this range, Sopris Peak is the most
northern summit. It rises abruptly from the broad, flat valley of Bear-
ing Fork to a height of 7,000 feet above it. It is a very massive moun-
tain, covering, with its broad spurs, an enormous extent of country, and
standing alone, as it does, is a very conspicuous and well-known land-
mark in all the surrounding country.
South of Sopris peak, the range lulls to a height little above the limit
of timber; this comparatively low ridge extends, with little change in
elevation, to Capitol Mountain, one of the crowning summits of the range,
whose gray, prism-sbaped top and precipitous sides forbid access.
A ragged spur running from Capitol Mountain northeastward separates
Capitol and Snowmass Creeks* It bears, near its end, a high summit,
27 H
418 GEOLOGICAL SURVEY OF THE TEBBIT0EIE8.
which has been named Moaot Daly, io honor of the gentleman who is
now president of the American Geographical Society. Two and three-
tenths miles farther south on the main ridge is the summit which has
been named Snowmnss Moant« This also is one of the highest saaimite
in the system, being but slightly inferior to Capitol Mountain in elevatioii*
It is a station in the primary triangniation. It has received its name
from an immense field of snow on its eastern face. This snow-field, in
August, which is the mouth when there is the least snow in the moan-
tains, had an area of lully five square miles. Probably this ia the
nearest approach to a glacier in the Bocky Mountains. These moon-
tains, Sopris, Capitol, Daly, and Snowmass, being of eruptive rocks,
are extremely rugged and precipitous.
Following the ridge farther south, it falls to an elevation of but 12,500
feet, which it holds tor. about six miles; then, on a sharp angle in the
ridge, rises Maroon Mountain. This peak is so named from its pecaliar
color, that of the sandstones of which it is composed. It is one of the
highest peaks in the system, and its summit is nearly, if not quite, in-
accessible. On the north and south it presents walls almost vertical
for 2,000 feet ; on the west it is full as steep for 3,000 feet, and €>n the
east a sharp, comb-like ridge runs down from its summit, forming the
commencement of a long, heavy ridge, which separates two large branches
of Eoariug Fork, Snowmass Creek on the west and Maroon Creek on
the east. This ridge has a direction nearly north, and for many miles
its crest is above timber-line, and it has several summits above 13,500
feet.
The main ridge, from Maroon Mountain, turns west for a few miles, with
two quite high summits on it in this part .of its course, then turns south
and suddenly falls considerably at the head of Maroon Creek, sending
off a heavy spur separating the two branches of Maroon Creek. The
highest point of this spur is near its end. It has been named Pyramid
Peak, from its peculiar shape. It is a first-class peak, reaching nearly
14,000 feet.
Farther down the main ridge, another spur with a sharp, ragged crest,
separates Maroon Creek from the next branch of Itoaring Fork, known
as Castle Creek. Castle Peak, from which this creek derives its name.
is the highest peak in the Elk Mountains. It stands on the dividing:
ridge, between the heads of two branches of Castle Creek. It has a
conical summit, from which the main ridge runs south, in a succession
of high, needle-like points, which rise several hundred feet above the
ridge, gradually decreasing in altitude as they recede from the main
peak. The summit is well-nigh inaccessible, the only way to reach it
being up a crevice on the south side. Its color is dark brown. A high,
sharp ridge, separating the two branches of Castle Creek, runs north-
eastward from this peak. Summits on this spur reach nearly I4,OU0
feet.
From Castle Peak this range runs generally about southeast for sev-
eral miles, bearing a number of summits of secoud-rate importance upon
it, to the junction with the Elk divide, as I call the ridge se|)arating the
waters flowing into the Gunnison from those flowing into the Grand.
South of this divide, the most important peak, perhaps, is the one named
Italian peak, which stands at the extreme head of the Gunnison River.
It was so named from the singular and beautiful grouping of colors on
its surface, produced by the red rocks, white snow-fields, and green
patches of vegetation.
South of Italian Peak, this range loses, in great part, its distinctive
character, has a less elevation, and becomes a mass of low, heavy spurs
GANS«TT.] GEOGRAPHY — ELK MOUNTAINS. 419
Across tbese heavy spars the Gannison makes it€( way, cutting a deep
caiion. On the sontb side of the river, at the head of the cauoD, stands
alone, a conical peak called Park Gone. This peak ends this range.
Farther south a rang^ of low hills connects with tbe range of the Gou-
tiDeutal water-shed. Tbe branches of East and Slaijte Rivers are sepa-
rated by broad ridges, rising bnt sligbtly above timber-line. Around
their heads, however, separating them from the beadwaters of Roaring
Fork and Bock Greek, is a higb, ragged ridge, set with lofty peaks, but
broken by low saddles. At the head of Teocalli Greek is a high summit,
known as White Itock Mountain, from tbe white, volcanic rock with
which it is capped. Between White Kock Mountain and Gastle Peak
there are several very high summits, none of them, however, exceeding
13,500 feet in altitude.
South of White Eock Mountain, on the ridge separating Teocalli
Greek from Dyke Greek, is a peak known as the Teocalli from its re-
semblance to tbe teocallis of the Aztecs. The strata composing this
mountain are nearly horizontal, and are so broken as to form a series of
steps from tbe base to the summit, a giant's stairway. The color of this
mountain is a dark-brown.
On the north side of White Bock Greek is a spnr separating it from
the head of East River, on which are a number of high summits ; also,
at the extreme head of East River there is a high peak known as Belle-
vue.
The ridge or spur separating East River from Slate consists of three
isolated mountains, separated from one another by low saddles. Tbe
northern one is known as Ginnamon Mountain, tbe middle one as Gothic
Mountain, from the spires and pinnacles in bas-relief upon its eastern
face, and the soathern one as Grested Butte. The latter peak standi)
entirely alone, in the angle of tbe two streams, and rises 3,000 feet above
the saddle north of it. This latter ridge is a part of a second range,
similar in direction to the eastern. Tracing it north of Slate Mountain,
it rounds the extreme head of Rock Greek by turning to the westward
for three miles. There it joins an enormous mountain mass known as
Treasury Mountain. In the south end of this mountain are the Elk
Mountain mines, and the name of the mountain is connected therewith.
This mountain extends, in a solid mass, in an east and west direction
live miles, and north and south three miles, to the junction of Rock
Greek with branch b. Between the months of creek a and b^ Rock
Creek is in close, heavy canon, cutting its way through this mass. On
the east side of Rock Greek, this mass, though still continuous, is more
cut up by streams, and shows several high summits, with oousiderabio
fall in the saddles. It connects, by a very high ridge, with the eastern
range. Its northern end is just west of Sopris peak, where a large
branch enters Rock Greek from the south.
The third range commences west of Sopris Peak, on the west side of
Kock Greek, in a ridge slightly above timber-line, which separates Rock
Creek from the upper valley of tbe North Fork of the Gunnison. This
ridge turns to the eastward, and crosses Rock Greek just above the
mouth of the creek, leaving only a comparatively low saddle, whose top
is about 2,000 feet above Rock Greek. This saddle is several miles
long, and terminates suddenly in an immense mass of eruptive moun-
tains, of which station 33 is a summit. There are a number of peaks
in this mass, of heights from 12,500 to 12,800 feet Some of the slopes
in this group are terrific. The west side of this mass rises straight up
from the plateau bordering North Fork for 2,500 feet, at an angle of 65o.
At the head of Slato River is the highest peak in this range. It has a
420
GEOLOGICAL SURVEY OF THE TEBBITORIES.
prism -sbaped sdmmit, very Bimilar to that of Capitol Monutain. Its
elevation is 12,891 feet. Thei*e are several suinmits near it, both in
position and elevation.
The next peak of importance in this range is station 32. This moon-
tain stands slightly detached from the range, extending into and partlj
across the valley of Anthracite Creek, which takes a wide detour to
get aroand it. It is composed of brownish-red, highly metamorphosed
slates. There are three sammits, of which the central one is the highest.
Farther down toward the sonth the range is very much div^infleti.
now high, now low, bat nowhere lower than 11,000 feet. It ends west
of Crested Bntte, in an isolated gronp of monntains, of an elevatiOD of
aboat 12,500 feet. South of this gronp there are two bits of sloping
mesa, and then the valley of the Gunnison.
West of this range the mountains decrease in elevation, and ooear in
isolated groups. Between Atitbracite and Coal Creeks there is a short
range, consisting of two ridges, connected by a low saddle, of about
10,000 feet iu elevation. These ridges contain several summits, ranging
in height from 12,000 to 12,000 feet. In the angle of Anthracite Creek.
and connected with the northern end of the range mentioned above, ii
a solitary peak, known to the prospectors as Mount Marcellina. Upon
its precipitous southern face are, iu bas-relief, Gothic spires, piedaely
as on the eastern face of Gothic Mountain.
Joining this range near the saddle, in the middle of its length, is
quite a heavy group of mountains. It sweeps quite around the head
of Ohio Creek, and contains many high peaks, several reaching nearly
13,000 feet. This gronp, in turn, is joined, by a low saddle, to a groap
which heads Coal Creek, of which H--34 is the highest summit.
From station 34 to stations 33 and 39 runs a well-defined ridge, hav-
ing an east and west direction. It contiects with the last-mentioned
group by a very low ridge, not exceeding 9,400 feet. This ridge ends
the system, and with it the Rocky Mountains in this latitude. West-
ward, to the Wahsatch^ range in Utah, stretches a system of enormoos
plateaus, iu which are cut the caftons of the Grand, Green, and Colo-
rado Rivers.
Rising on the north fk*om the valley of the Gunnison River and ilR
Korth Fork, was originally a |*reat plateau. Its limits were, on the
west, about in longitude 108^ 15'; on the south in latitude 38^ 45'. Ii
extended cast nearly or quite to the Elk Monntains, and north to tiie
Grand «River. Its elevation, in its eastern part, is about 11,200 feet,
an elevation still held by a few isolated points of traohyte. The ele-
vations of a few i)oints on its surface will give an idea of the direction
and amount of its slope.
• • » -
Latitude.
Longitude.
Station 44
Station 43
H-39 :
Station 42 (not the original surface)
Station 45 ,
North Mam
Soath Mam
23-45
24-45 ......•..^. ..;.•> ^wv. — «k4.^...r^.»4.. «.«<
4-39 ,.^ ,
North end of plateau, (station 54 ) 1
South end of plateau, (station 59)
3
2
1
0
5
3D
39
:»
39
39
39 23
^ 22
39 23
39 .23.,
39 4
39 G
38 53
107 41
107 40
107 40
107 45
107 50
107 51
107 51
107 55
107 57
107 50
10i5 13
106 10
E^evatlM.
Ftet.
Il,l5^
ll.i:M
iu.c.«
io,a">«
lO.Pitf
lo.cir
10,tft
10, 0£
10, 90"
9,i»^
9,7$^
OAXSETT.] GEOGEAPHW-EAGLE RIVER. . 421
As win be seen, the direction of the B\o^e i& from the east toward the
westi and is tolerably uniform, being about 50 feet to the mile.
The original basalt capping of the plateau has been in great part re-
moved by denudation, appearing only iu points and ridges, here and
there^ except in the western part, where a large area, of 75 square miles,
preserves the original surface, and is as level as a floor.
This plateau has been cut in two pieces by a large creek, an afSuent
of the Grand Biver, which I have named Plateau Creeks It has cut out
for itself a very broad valley, of a depth, in its deepest part, of 6,000
Iteet below the level of the plateau. With the aid of the Grand Itiver
on tJie north, it has cut down the western extension of the part of the
plateau north of its valley to a range of low mountains. They are ex-
tremely rugged and precipitous, of elevations from 7,000 to 10,000 feet.
The Grand Biver has its head in the eastern part of Middle Park,
across which it flows, receiving, on its way, several large branches.
It cats its way through the Park range on the western side of Middle
Park in a very heavy canon. In latitude 39o 39', longitude 107o 3', it
receives the waters of one of its largest tributaries, the Eagle Biver.
This stream heads in Tennessee Pass, and the mountains of the Park
and Sawatch ranges. In that neighborhood, near its head, it flows
through broad and beautiful meadows, which would be valuable for
agricultural purposes and for stock-raising, but the elevation, over 9,000
i^t, is too great fov the former, and also for the latter, except during
the summer.
The river receives, in these meadows, a large branch from the east,
aud^ in the caiion, at the foot of these meadow(«, a large branch from the
southwest and another from the east^ by which its volume is very much in-
creased. The branch from the southwest heads'under Oomestake Peak,
so named from the Homestake mine, which is situated at timber-line ou
its southeastern slope.
Eagle Biver, below these meadows, is in close, high cauon for about
Ave miles, emerging therefrom at the mouth of lioche Moutonnde Creek,
into a narrow valley, inclosed by high, precipitous walls. The spur
from the continental divide, of which the Mountain of the Holy Cross
is the most northern as well as the highest i>eak, gives rise on the east
and uotth to branches of the Ragle. Biver, and on the west to Frying
Pan Creek, a large branch of Boariug Fork. . From this mountain mass,
the spurs separating branches of the Eagle Biver have a broad, plateau-
like character, sloping at a low ang!e, the ends forming the west^wall of
the canon, and of the narrow valley below. These branches of the
Eagle Biver are all in close caQon.
Below the mouth of Boche Moutonni^e Creek, the river remains in a
narrow valley as far down as the mouth of the Piney Ci*eek, a branch
Irom the east, nearly as large as the Eagle Biver itself. Below the
mouth of this stream the valley broadens to nearly two miles iti width ;
but this is mainly bench-land, with a gravelly soil, covered with sage,
and can be of use only when irrigated. There is sufficiept bunch-grass
to afford indifferent grazing. The hills rise abruptly from this valley,
and then extend back in long ridges to the mountain mass spoken ot'
above.
The course of the river commenced to cliange near the mouth pf Bocbo
Moutonude Creek, from north toward west, and at the foot of this valley,
that is, near the mouth of/ creek, has a course nearly west. Uere it
enters a caiion, which extends as far as station 7, where it ends abruptly,
and the river flows through a broad valley, which extends nearly to
its mouth, and far up g creek. This valley, like that above, is covered
422 GEOLOGICAL SLTIVEY OF THE TERRITORIES.
mainly with fia^e, but, if irrigated, might prove prodactive. Tbe soil,
liowever, coDtains some alkali, g creek has a broad abd fertile bottom.
Between these two valleys, the ooantry consists of rolling hills, covered
with excellent grass.
From the mouth of h creek to its mouth, the Eagle River is iu dose
cafioD, and the junction of the rivers is iu this caiion, which extends down
the Grand to the mouth of lioaring Fork, with little intervals of valley.
Its height is greatest fifteen miles below the mouth of the Eagle River,
where it reaches 9,400 feet. This caiion is cut in a rolling table-land, of
an average elevation of 9,000 feet, which separates the water of Eagle
Kiver from that flowing into Koaring Fork. It is well watered, sparsely
timbered with quaking aspen, with plenty of excellent grass. It is too
exposed and the elevation is too great for a winter range for stock, bat
for a summer range it is excellent.
The divide between the waters of the Eagle and Grand Rivers on tbe
north, and Frying Pan Creek on the south, consists of a broad, flat-
topped ridge, whose summit is slightly above timber-line. It joins the
Sawatch range near the Mountain of the Holy Cross. Thence it has a
course nearly west to Roaring Fork.
Roaring Fork takes all of the Grand Biver drainage on the northern
slopes of the Elk Mountains, and the western slopes of the . Sawatdi
range, north of the Elk divide. Its branches, without an exception of
any consequence, head among the high peaks above the limits of tinn-
ber, and most of them have their entire courses in the mountains. The
lower course of Eoarins: Fork, that is, below the mouth of Castle Creek,
is in a valley gradually increasing iu width till it reaches its greatest
width at the mouth of Bock Creek, where it is fully four miles wide.
The bottom-land, as almost everywhere in the Territory, is excellent,
and is unusually broad, but liable to sudden overflows from the melting
of snows in the mountains.
Grand Biver, below the mouth of Boaring Fork, is in a narrow val-
ley, with very high hills on each side, (rising abruptly,) for abont three
miles. Then it enters a close canon, in which it is for twelve miles,
when it issues from this canon into a broad valley, east of the Korth
Mam plateau, as I call the portion of plateau between Plateau Gre^
and the Grand Biver. Tbe country south of this cafion of the Grand,
and west of Bearing Fork, consists of high, rolling hills, covered with
a heavy growth of cottonwoods. The elevation of summits in this
mass oi' hills exceeds 10,000 feet.
The oroad valley, alluded to above, extends down the Grand to tiie
2^orth Mam plateau, nortli of the river to a considerable distance, and
south of it ten miles, speaking generally. Within this valley the Grand
receives three branche's of considerable size. The largest of these,
which I have named Uivi<le Creek, comes into the Grand just west of
station 22.
The principal, almost the sole, production of this valley is sage. There
is no grass, ej^cept iu the stream bottoms. The soil is extremely poor.
The hills farther south, which rise to the Gunnison and Grand divide,
are covered densely with scrub-oak and smaller bushes, with some quak-
ing aspen.
In passing the North Mam plateau and the Plateau range, the valley
of the Grand is very much contracted, averaging not more than live
miles in width. In this part of its course, tlie river is very sluggish and
winding, with numerous bayous and islands.
Opposite the North Mam plateau, on the north side of the river, the
country consists of a rolling plateau, extending as far to the north aiMi
cAKK£Tr] GEOGRAPHY GBAND RIVER. 423
west as the eye can reach. The cliffs on the south edge of this plateau
are perpendicular, and even in places 6verhanging, and the tops pro-
jecting, so that, at noon. in August, they cast a shadow on the vertical
wall beneath.
Below the Plateau range, the valley widens immensely. This valley
is not more inviting than the one above the North Mam plateau.
In latitude 39° .08', longitude 108o .19' the Grand is crossed by the crest
of a range of hog-backs. This crest has a general direction slightly west
of north and east of south. The dip is toward the east, and is slight,
and as the Grand does not cross this range in a direction contrary to
that of the dip, but obliquely to it, the caiion which it cuts is very long,
being about 15 miles. It increases in depth very gradually, until,
at the lower end, it is about 1,800 feet. The western edge of this line of
hog-backs is nearly vertical, and the exit of the river from the canon is
very abrupt. The surface of this hog-back is very much broken and cut
by sidecaiioDS.
Plateau Creek heads in the eastern part of the plateau, and about mid-
way between the Grand and Gunnison Rivers. It flows tin^t northwest,
down the slope of the plateau, cutting deeper and deeper. At station 49
its course changes to west, and it holds this course very constantly to its
mouth, in the middle of the Hog-back Caiion. This plateau has an
enormous amount of drainage. Near its toi> the valleys are broad, flat,
and marshy, with numerous small lakes or ponds. The best land in the
district for agricultural and stock purposes, is that on and near the tops
of the high mesas ; but the great elevation precludes their use for these
purposes.
Plateau Creek drains the whole of the northern slopes of the main
plateau and the southern slopes of the Noith Mam plateau. All the
streams flowing to it from the main plateau have a course nearly due
north, forming a very regular system of- drainage. The valley of this
stream is, throughout the greater part of its course, quite wide," with, in
places, enormous extents of bench-land between its branches.
At the foot of Hogback Canon the Grand emerges into a broad valley
in which it meets the Gunnison. This valley is of enormous extent,
stretching far down the Grand, even beyond the Sierra la Sal and up
the Gunnison ten miles above the moiith of the Uncompahgre River,
and up the Uncompahgre for at least forty miles. Its width, on the
Grand, below the mouth of the Gunnison, is about ten miles. It is
bordered on the northeast, for some distance, by the range of hogbacks
mentioned above; on the i^outhwest, by a plateau lower than that
described above and of a different character. . The Grand hugs closely
the edge of this plateau. The river- bottom of the Grand is upward of a
mile in width, weH timbered with cottonwoods, and very fertile. The
rest of the valley is bench-land, elevated about 100 feet above the river,
at the edge, rising very gradually toward the range of hog- backs. The
soil is gravelly, with much alkali, and produces only greasewood and
sage.
The part of this valley included between the Grand, the Gunnison,
and the west edge of the great plateau is nearly triangular in shape,
the two rivers and the edge of the plateau forming the sides. It al8<»
extends up the Gunnison, east of the western edge of the plateau, to
longitude 107^ 55'. The area' of this pai-t of the valley is three hundred
square miles.
The western edge of the great plateau consists of a precipice of basalt,
averaging 200 feet in height, below which there are timbered ridges
424 GEOLOGICAL SUBV£Y OF THE TEREITORIES.
ranning down into the valley, and terminating in tongues of sloping
mefia.
Between longitnde lOTo 55', and the month of Boobidean's Creek,
the Gnnnisoa occupies the bottom of this valley, with a fertile bottom
upward of two miles in width, in which the river is very sluggish and
winding, with numerous sloughs and backwaters. Below the month of
lioubidean^s Creek the river does not occupy the lowest part of the val-
ley ; the latter lies between the river and the great plateau, aboat three
miles, generally speaking, east of the former, and follows its general
course. From this lowest part of the valley the land rises slowly towmd
the west, and, in a caiion, which originated in a monoclinal fractnie,
closely hugging the plateau on the west side of the valley, the Guunison
has its course. This canon, known to the Indians as the Unaweep, is in
stratified rocks, of the most brilliant colors. It has an average depth
of about 800 feet, with walls absolutely vertical. The river-bottom is
quite broad, and the river is sluggish and winding, now undermining
one wall, now wandering across the broad and fertile bottom to the
other. The soil in this bottom must be excellent for agricnltaral por-
poses.
The remainder of this great valley lies on the south side of the Gun-
nison River, extending up the Uncompahgre Eiver for upward of forty
miles, with an average width of eighteen to twenty miles. On the west
it rises gradually into a plateau. On the east it is limited by the plateav
in which the Grand GaSion of the Gunnison is cut, and by spnrs from
the Uncompahgre range, and on the south by this range. The stream-
bottoms in this part of the valley are, as in the other, very fertile,
and quite broad, with a heavy growth of cottonwoods. The rest of
this portion of the valley consists of perfectly flat bench-land, rising
in regular steps from the streams to an elevation of about 200 feet above
them. Throughout the valley 'the bench-land is very poor, with a clay or
gravelly soil, containing always some alkali, and in many places strongly
impregnated with it. There is very little grass, indeed. Sage, grease-
wood, and several species of cactus, form almost the sole ^^getation.
A great deal of the water sinks, so that, except in the spring, only the
larger streams contain any water, and the water of the larg^ streams
is more or less ledkaHne. Betweein the Grand and the Gunnison, Elahnah
Greek and b creek (of the Gunnison) are almost the only streams
containing water in October, and, south of the Gunnison, the Uncom-
pahgre is the only stream in the valley which is not dry at that time of
the year. Gedar Creek and lioubideau's Creek are dry. It is in this
valley of the Uncompahgre and the Gunnison that the Utes asuaUf
have their winter quarters.
The Gunnison River heads under Italian peak, and its upper branehes
drain the sonthem slopes of tl|6 Elk Mounttdns and the western alopai
of the Sawatch range. The branches whidi drain the Elk Moantaiiw
have a general direction of -^^P east of south, as is the ease with Slate
River, East River, Ohio Creek, and the numerous parallel streams west of
Ohio Creek. The main stream is in a narrow valley for several miles below
its head, extending nearly down to the mouth of Pass Creek. Thenoe
to Park Cone it is in a broad valley of gravelly soil, which is mainly a
glacial deposit. At Park Cone, it enters a caiion, by which it cuts its
way through the eastern range of the Elk Mountains. Thiscanoois
cut in granite, is sixteen miles long and is, on an average, l,2U0fee(
deep. In this cafloB, a iarge branch, Taylor River, enters uie Gnnnlsoa
from the north. Just below its foot, the next large tributary. Slate
River, comes in. This stream and its tributary, East River, drain a
ojkxxETT] GEOGRAPHY — GUNNISON rIvEB. 425
large part of the Elk MoimtaiDS. Moat of tbeir brHDcbos have tbe usnal
directioD, and are in narrow valleys, with heavy, massive ridges between
theui. The longer pan of Slate Kiver, from Crested Eutte to its montii,
is in a valley two to four miles in width, of the same character as that
on the Qunnison alK>ve tbe canon. This valley extends down the Oun-
uison to tbe mouth of Oochetopa Creek, with a width of abont five miles.
The river-bottom of tbe Gnunison in this part of its course is quite
broad, and densely overgrown with bushes and eottonwoods*.
Between Slate Biver and Ohio Creek, south of the termination of tbe
mountains, are two rather remarkable pieces of table-land. They evi-
dently were originally but one, but have been cut in two by erosion.
Tbeir surface slopes considerably toward the Gunnison.
At the junction of Ohio and Cochetopa Creeks with the Gunnison,
tbe valley is very broad, extending far up Ohio Creek, with a broad
bottom on each stream. In this valley, between tbe Gunnison and
Cochetopa Creek, is located the embryo town of Gunnison. This town
was started by a company, on the colony plan. Thus far it has not been
a anccess, principally owing to its great distance from other settlements,
and the limited means of communication. The situation is excellent,
tbe soil very good, and, with the aid of irrigation, it will produce good
crops. Tbe range i'or stock, both for summer and winter, is not excelled
in the Tenitory. This range now supports, throaghont the year, the
6t€x;k belonging to tbe Ute Indians of the Southern or Los Piuos agency,
numbering about 900 head.
Below the mouth of Cochetopa Creek, tbe valley narrows to about a
mile in width, which is all bottom-land, and which extends about four
miles down the river. North of it the country rises, in a sloping pla-
teau, to the Elk Mountains. This plateau is cut into long tongues by
parallel streams — branches of tbe Gunnison. At the foot of this valley
these long tongues of mesa run down to the river, forming a caSon lOO
to 200 feet high, which extends, broken at intervals by bits of meadow-
laud, as far down as the mouth of g creek. On the south side, the coun-
try' is very broken, but in general rises gradually toward tbe Uncom-
pabgre Mountains. %
West of the mouth of g creek tbe land rises rapidly on both sides of
tbe river, into a high plateaa. This plateau, on tbe south side of the
river, is almost perfectly flat, with an average elevation of 9,000 feet.
On the north side it slopes upward toward the northwest yery gradu-
ally. At the river it has the same elevation as on the south side. It is
in this plateau that tbe Gunnison cuts a part of its great cailon, a cation
fifty-six miles long and 3,000 feet deep in its deepest part. This plateau
consists of gneiss, topped with 1,000 to 1,200 feet of stratified rocks, in
beds nearly horizontal. The cailon is cut through the beds of stratified
rocks, and deep into tbe i^oeias, tbe deptb of tbe eafion in tbe gneiss
inereasing with the fall ef the river. This part of the cafion has rough,
lugged, nearly vertical walls, with no beaoh to the river. On top of the
gneiss there is a slopiug bench, marking the line between gneiss and
stratified rocks. Above this bench are the steeply-sloping walls of strat-
ifi(Ml rock, generally ending with 100 or 200 feet of perpendicular clifi'
just below the summit of the mesa. Tbe tributaries of the Gunnison
in this plateau cut but slightly into the gneiss, consequently these
streams have a very rapid fall just before reaching the river. The top
of this plateau is well watered, covered with excellent grass and groves
of qaaking aspen. It is a moat excellent aommer-range for stock, but
the elevation is too great to allow of its use as a winter-range.
At stations 77 and 78, the character of the plateau changes, as far as
426 GEOLOGICAL SURVEY OF THE TERRITORIES.
the north side of the river is concernecl. The flat plateaa ends in a very
well-defiDed terrace, oq an enormous scale, ten miles long and 1,800 to
2,000 feet high. In its place there is a lower sloping plateao, or long
hog-back, with its edge at the Gunnison Biver, and line of greatest de-
pression in the valley of the North Fork of the Gunnison. This is a
true sloping plateau, its surface being perfectly flat and unbroken, with
the exception of the cafions of Smith's Fork and Dry Caiion, which have
a course nearly parallel to that of the Gunnison above station 80. These
streams have many small gullies coming into them from the soatb, bat
none at all from the north. The line of greatest slope of this plateau has
a direction slightly west of north. This plateau contains no water, aud
the vegetation consists of the piiion pine, cactus, sage, and scrub-oak, a
marked difference in character from the plateau just east. This differ-
ence is owing in part to the greater slope of this plateau, thus carrying
the water off' more rapidly, and in part- to the less elevation. The
highest part, the edge, at the caiiou of the Gunnison, is 8,600 to 9,000
feet, while the valley of the North Fork, the lowest part, is 5,400 feet.
The character of the cailon on the north side, as far down as station
80, is similar to that above, both geologically aud topographically.
The stratified beds occupy 1,000 to 1,200 feet, with the same marked
bench, and the precipitous cailon in gneiss below. On the south side,
however, the top of the caiion is lower than it is above station 77,
and the caiion is cut entirely in gneiss. The plateau on the south side
is nearly horizontal, with a slight slope to the west.
At station 80 the river turns abruptly toward the north, aud flows
in the direction of the greatest slope. Between station 80 aud the
mouth of tbe North Fork it has most of its fall. On the east side of the
river the character of the canon is not materially changed until the
mouth of Smithes Fork is reached. On the west side, however, the
plateau ends abruptly opposite station 80, and a hog- back ridge of
stratified rocks, dipping steeply to the west, forms the upper part of
the west wall. This wall is much loweri^han that on the east, and is no-
where more than three miles thick. Beyond it is the broad, flat valley
of the Uncom^ahgre, at as low or lower elevation than the Gunnison.
Between stations 80 and 81, the two parts of the caiion are very
strongly marked, showing a canon wit>hin a caiion. The caiioa in
gneiss is merely a narrow cleft in the rocks, with smooth, vertical sides,
between which the river rushes down, its surface white with foam. At
the mouth of Smith's Fork, the cailon i4i gneiss is but 300 feet deep,
while the stratified rocks lise up to nearly a thousand feet. Just below
this point it runs out of the gneiss, and the rest of its course is in strati-
fied rocks, in which its character is entirely different. It no longer
nishes madly along, but meanders about in the broad bottom from one
wall to the other, leaving, now on this side, now on that, broad patches
of l>eautiful bottom-land. This character of caiiou, similar to the lower
or Uuaweep Canon, continues as far as station 83, where it termioates
abruptly.
The appended list of elevations in different parts of this caiion give
an idea of its dimensions:
Height of the walls of the Grand Canon of Hie Ounnison^ at different poii^
A t the head, near the mouth of Mountain Creek :
F«et
At level of the river a 7, 200
Top of plateau on north side of the river t 8, »00
Height of caiion wall 1, 6(K)
GAssETT.j GEOGEAPny — GRAND CANON OF THE GUNNISON. 427
At the month of / creek T
At level of river est 7,^00
Top of the gneiss a 8, 000
Height of e«fion in gneiss 900
Top of plateau, east side /creek a 9,000
Ileight of cafion wall 1, 900
Top of plateau, west side / creek a 8, 900
Height of canon wall 1,800
At station 77 :
At level of river fc C, 800
Top of gneiss, north side of river a 8, 600
Height of canon in gneiss 1, 800
Top of plateau^ north side of river, (station 77) a 9, 800
Height of canon wall 3, 000
Top of plateau, sonth side of river t 9, 400
Height of canon wall 2, 600
At station 80 r
At level of river ..., est 6,200
Top of gneiss, northeast side of river est 7, 200
Height of caiiou in gneiss ^ 1, 000
Top of plateau, northeast side of river, (station 80) a 8, 500
Ileight of canon, northeast side 2, 300
Top of platean, southwest side of river i . . # 8, 050
Height of canon 1, 850
At mouth of Smithes Fork :
At level of river .,., est 5, 600
Top of plateau, east side of river, (station 81) a 6, 437
Height of caiiou, east side 837
Top of plateau, west side t 6, 700
Height of cafLou, west side 1, 100
At mouth of North Fork :
At level of river •. a^5, 400
Top of plateau, east side, (station 82) a 5, 800
Beight of caiion, east side 400
At foot of canon :
At level of river a 5, 125
Top of plateau, (station 83) a 6, 750
Beight of canon 625
The North Fork of the Gunnison is its largest tributary. It drains
nearly all of that part of the £]k Mountains west of Bock Creek, which
consist principally of the isolated groups which have been described
earlier in this report, and of most of the southern slope of the great
plateau. Those of its branches which drain the mountains have no
valleys worthy of mention within the mountains, and outside of them
are in close caiion. The main stream heads against the divide between
the Grand and Gunnison Rivers, in longitude 107^ 30', and drains a
very broad valley. It enters a caiion in the rolling plateau country, in
latitude 39o.4^ and in this caiion receives the branches known as Anthra-
cite and Coal Creeks. This caOon continues as far down as the longitude
of station 39, where the stream comes out into a valley, which is very
NcrrK. — bf barometric nmasurement ; a, aneroid measnromeDt ; f, trignometric meaa-
nrement; eei.f estimated.
428 GEOLOGICAL SURVEY OF TDE TEBBITOEIES.
similar to that of the Uncompah^e. This valley is at tbo foot of the
sloping plateau in which is cut the Grand Caiion of the Gunnison. This
stream enters a low caiion, just above its mouth, in which it enters the
Gunnison.
DISTRIBUTION OF VEGETATION.
Vegetation, in its character and abundance, is modified by several
causes. Elevation above sea-level is, perhaps, the most powerful in
determining its character. The nature of the soil, amount of moisture,
&c., are, of course, very powerful iu influencing it. The general char-
acter of the vegetation as influenced by hight is as follows: The stream-
bottoms, up to a height of at least 8,000 feet, produce abundantly oot-
tonwoods and grass. The soil is deep and rich, and there is abundant
moisture. The lower bench-land, up to a height of fully 8,000 feet,
produces principally sage and greasewood, piilon pine, yucca, and eae-
tus, with more or less bunch-grass. The soil is gravelly, or an alkalioe
clay, dry and arid. The upper benches and lower mountain slopes an
covered with scrub-oak, piOou pine, wild service-berry and other boshes.
This kind of vegetation is found at elevations from V,000 to 10.000 feet
above sea-level. The soil is quite dry, though not as dry as the last
From 10,000 to 11,000 or 11,500 feet, i. c, to timber-line, on the mount-
ains and plateaus, the characteristic vegetation is iiine and spruce, with
excellent grass. At these high altitudes the soil is very well watered.
SETTLEMENTS, TRAILS, ROADS, ETC.
Settlements west of the Sawatch range are very few and small. ITii*
only practicable way of reaching the country with wagons is by a long
detour to the south, via the San Luis Valley and Cochetopa Pass, as
none of the passes in the Sawatch range are practicable for wagons.
Besides the embryo town of Gunnison, mentioned previously in this
report, settlement is confined to a few mining camps in the Elk Mount-
ains and the valley near the head of the Gunnison. There are small
camps on Texas and Batty Creeks and in Union Gulch, near the hciid
of the uppericaiion of the Gunnison, working placer-deposits. At the
head of Rock Creek, iu the south end of Treasury Mountain, there is
a camp of miners working quartz-leads. Washington Gulch has been
worked, but is now abandoned. A small camp has been located on 0-
be-joyful Creek during the summer of 1874.
The whole of the area west of the one hundred and seventh meridian
is within the reservation of the Ute Indians.
The only wagon-trails are from Gunnison up the Gunnison River and
East River to the mining camps in Treasury Mountain and the trail
made by Captain Gunnison In 1854, referred to above. This trail,
though very rough and difficult, is occasionally used now.
Trails are abundant, lending iu every direction, so tbAt it would be an
endless work to particularize them. The main trail connecting th^ Lo8
Pinos and White River Indian agencies passes up Ohio Creek to its head,
descends Anthracite Creek, ascends the North Fork, and follows
Divide Creek, to its mouth, where it crosses the Grand. A heavy trail
follows the Gunnison River from the mouth of Cochetopa Creek to its
mouth on the north side. The great plateau is crossed by many trails,
and nearly every stream has a trail along it.
CHAPTER II.
ELEVATIONS.
Blevations Lave LeeD measured by cistern barometer, aneroids, and
tbe vertical circle of the* gradienter. Most of the mountain summits
in the western part of tbe Elk system and on tbe great plateau were
measured trigooometrically by the vertical circle of the ijradienter,
based on the barometric elevatious in the eastern part of tbe system.
BEVISION OF THE HEIGHTS OF SUMMITS IN THE SA WATCH AND ELK
SYSTEMS.
•
¥or a more accurate determination of the elevations of these monnt-
ains, I have employed a combination of the barometrical and trig-
onometric methods. By means of the vertical angles, between the peaks,
their relative elevation has been determined with considerable accuracy.
Then the heights of the several peaks, as measured by barometer, are
reduced to a common point by use of these relative elevations. The
mean of these results, giving suitable weights, gives a mean elevation
for this common point, and, applying to it the difference in elevation,
gives the heights of the other peaks. The accuracy of the results depends
on the character of the leveling, the number of barometric elevations,
and situation of the barometric base to which they are referred. In the
iSawatch range, within the area over which I worked during the season
of 1873, four peaks were measured by cistern-barometer. The barometric
observations on these peaks were referred for a base to those taken near
the summit of Mount Lincoln, at an elevation of 14,194 feet. The dif-
ference of elevation in no case exceeds 400 feet, and the greatest distance
(to Mount Princeton) is forty-two miles, while the least (to La Plata
Mountain) is but twenty-nine miles.
In the Elk Mountains five peaks have been measured by cistern -barom-
eter, and referred to Mount Lincoln as a base. Of these the nearest
to Mount Lincoln is Italian Peak, forty-four miles from it, while the one
farthest off is Crested Butte, which is at a distance of fifty-five miles.
The greatest difference in elevation is more than 2,000 feet
The following is a nummary of the work of reduction of the barometric
elevations in these two monutainsystems, with the resulting elevations:
* Satca'ch range.
1a Plato Monntain
Grir.8l.v Peak
Mount llan'ard . . .
llounl Pnucctou . .
Relative ole-
vatiou.
Feet.
0
— iJ55
-113
Elevation of
barometer.
Feet.
U,3?9
1 i, rcw
14.:i84
Elf>vation of
La Plata
Mountalu.
Feet
14.303
1<,3I7
14,390
1 1, :U4
MeoD rltfva-
tiou.
F4et.
14.311
13.050
14. 375
14. 11)6
4*^
430
GEOLOGICAL SURVEY OF THE TERRITORIES.
In taking the mean of the elevations of La Plata Monntain, a dooUe
weight has been given to the result trom the barometrical observadoo
taken on this mountain, as it does not depend on vertic^il angles.
The small range of results on La Plata Monntain (only 18 feet) demon-
strates the excellence of the Mount Lincoln base, and the importance of
having the base as nearly as possible at the same elevation as the points
measured.
From these points as bases the following heights have been measared,
each result being the mean of a number of vertical angles taken with
weights inversely proportional to the distances:
Feet.
Massive Monntain (highest snmmit) 14,298
Mount Elbert (northern and highest summit) *. 14,351
Mount Yale 14, l"**
Station 75 13,2M
Elk Mountains,
SnowxDass Moantain..
Castle Peak
Crested Bn tte
White Bock Monntaiu
Italian PeAk
Relative ele-
ration.
Feet.
0
+145
— 1,»I8
— GI3
—620
Elevation of
barometer.
Fut.
13,061
14. 11)6
13.014
13,423
13.284
Elevation of
Snowmasa
Moantaio.
13.961
13.961
13,933
14,036
13,904
MeaneleT>
tioD.
Fvti.
13, 9^
14,115
13.^7
13,3J0
As before, doable weight was given to the direct barometrical resalt
on the common point, in this case Snowmass Monntain. The resalting
elevations show mnch greater range than in the Sawatch system, as
might be expected from the greater distance from the base, the great
range in elevation, over 2,000 feet, and the fact that the great Sawatcli
range lies between these mountains and Mount Lincoln.
From these peaks as bases, the following elevations have been meas-
ured by vertical angles, each result being, as before, the mean of several
independent measurements, giving suitable weights :
ELK MOUNTAINS.
EA8TBRK RANGE.
Capitol Mountain
Maroon Moantain
MoQDt Daly
Pj'raniiil Peak
Sopris Peak
Teocalli Mountain
Station 63
Park Cone
Snowmass Monntain
Castle Peak
White llock Mountain
Italian Peak
liellovuo Mountain
Between forks of Castle Creek
Do
Latitude.
i
Longitude. 1
O 1 II
O / '/
39 9 0
107 4 40
39 4 30
106 59 80
39 11
107 4
39 5
106 57
39 15 54
107 9 50
38 57 4U
106 53 0
38 54
106 30
38 46
106 36
39 7 13
107 3 44
39 0 30
106 38 40
38 58 30
106 55 10
38 56 35
106 45 0
39 1
107 1
39 13
107 4
39 13
107 3
39 2
107 3
39 3
107 0
39 0
106 53
39 8
106 53
39 4
106 51
39 5
106 51
39 6
106 4tf
Eleratkn.
13,997
HOMi
13. IW
13, e»
\%&\
uin
13, «4
UWl
UWJ
14,115
li.357
13, 3»
18.3:0
13.050
UOOO
13.340
13,030
U400
W.1«0
12. W
D.ao
CSJkNNETT.]
GEOGR APIJ Y — ELEVATIONS.
431
SetTreen CaBtle and Maroon Crcel&a
1II0DI.£ RAXOC
Crested Batto
Oothic MonDtain
StAtionGO
Xreasury MouDtain
Oinnamon Moantain
Sod of ridge north of last two points . .. .
Top of Kock Creek Cafion. north side
WE8TSRN KAXGK,
Station 30
Station 33
Station 33
Slate Moantalu
Station ii0
BCATTSRED OROUFB.
Jtfotint Marcellina
StatkMiSl
Station 34
Station 30
Station 36
Latitude.
Longitodc.
Elevation.
Q 1 If
O 1 II
Feet.
30 S
106 54
13.150
30 3
1C6 46
12,330
30 0
106 47
13,550
38 58
116 47
12,750
30 7
106 50
13,230
30 6
106 f 8
12.{K)0
30 2
1U6 54
13,150
30 1
106 58
13. 200
30 0
106 58
13, COO
38 53
106 56
13, 053
38 57
107 0
12, 570
30 0
107 4
12. 203
30 1
107 6
13,800
30 0
107 3
12,600
30 8
107 10
13.750
30 7
107 0
li,470
30 13
10? 11
12,050
30 5
107 6
11.682
30 4
107 7
11, 430
38 48
107 3
11,073
38 dO
106 50
13,300
38 40
106 50
12, 310
38 40
106 58
12,250
38 40
106 57 30
12. OOi
36 48
106 57
11,547
38 55
107 7
12,060
:o S
107 15
12,481
30 4
107 17
12.613
30 3
107 17
12, 578
30 0
107 6
12,8<»l
30 0
107 10
11.582
38 53
107 3
12,220
38 5:5
107 3
13.23U
38 56
107 14
11.324
23 52
107 16
12. 176
38 51
107 15
12, 003
38 51
107 14'
12, 312
38 51
107 13
12,2j0
38 50
107 13 30
12,238
38 43
107 13
12. 0.20
38 4*2
107 U
12,841
38 43
107 13
12, 861
38 43
107 0
12.468
38 45
107 18
12, 746
3d 43
107 23
11, 740
38 44
107 23
11,715
38 40
107 23
12,088
38 45
107 W4
10.838
38 48
107 31
ll.;«7
38 46
107 33
10.634
•i^ 41
107 25
10,877
38 47
107 28
11,713
3d 47
107 20
11,613
1
432
OEOLOOICAL SURVEY OF THE TERSITORIES.
ON THE PLATEAU.
GRKAT TLATEAU.
Station 43
Station 4:)
6tatiou44
SUtion43
JSorlh end of platean
Soutli OQil of plaiteau
NOUl n MAM ri^TEAU.
North Main
8ualh Matu ;
I'LATKAU BAXGE.
Station 50
LatiXnde.
30 23
39 S3
3Q )t3
39 SO
39 19
39 18
39 17
30 Ifi
39 16
*a9 17
LoDgltadeL
o
/ //
o
■ f
30
0
107
45
30
8
107
40
39
3
107
41
39
1
107
40
39
4
107
M
39
5
lUT
50
39
C
108
13
38
53
106
10
108
108
108
108
108
106
108
it
107 51
1U7 51
1(7 55
107 57
9
1
4
6
7
8
Fttt
10^ <e
11,134
II, lie
11,M
10, 901
10.954
9.800
9.^3
10.93
lOL^n
10.ttl
10. 6D
9.006
7.M5
7,M
7.90
8.8:5
8. OK)
8,643
Approximate latitudes and longitudes of other important points.
Ten oessce Pass ,
Lake Creek Pass
Moutli of Lake Creek
liloiith of Cottonwood Crvek
Month of Eagle Klvcr
Mouth of Roarinc: Fork
Mouth of Slate River
Month of White Earth River
Mouth of Cochetopa Creek
Month of Lake Fork uf the Guouison River ..
Month of CebolU Crock
Mouth of North Fork of the Guunison River.
Mouth ot Uncompabsre River
Moutli of GuDDison River
Mouth of Plateau Creek
Latitodo.
Longitude.
o
1
o <
39
iM
IOC 19
38
\^
106 33
39
5
106 10
38
50
106 7
39
'X\
107 3
39
31
107 10
38
4'i
106 SO
38
29
107 13
3b
sa
106 he
38
97
107 91
W
88
107 XI
38
47
107 »
38
45
106 5
39
4
lOd 33
39
11
lOd 16
GRAND RIVER.
3Iilea from
month of
Gnnniaon
River.
(;nind Lake, Middle Park
Mouth Blue River, (homl of cafion)
Fotit of caQon in Park range
Mouth of £a;;lo River
Mouth of a creek
Mouih of Roaring Fork
Mouth of rroek ,
Month of North Mam Creek
Mouth of Guunison River
884
178
171
114
110
95
89
75
0
Slevfttion.
FuL
8.153
7. 183
7,00J
6.1S5
6.0UO
5,TJ4
5,645
5,445
4,583
Pan per
mile.
FfA
8L1
lit
31-«
17. ■;
14.3
1&3
O-AXNXTT.)
OEOGBAPHY— ELEVATIONS.
433
KAGLE BIVEB.
Milen from
xnoutli.
TFennesaee Paaa, (bead)
!ldouth of Homestako Creek
JUCouth of Roche Moutonn6e Creek
Iklouth of piney Creek
^iomh/ creok (head of cafioD) ...
Jdoath^creek
SAoaibAcreek
^outb
62.0
b0.0
4j.O
41.0
29.0
13.0
6.5
0
ElevAtion.
Feet
10,418
8,093
7,856
7,70J
7, 005
6*601
0,389
6,1:25
Fall per
iLile.
Feet
143.8
167.4
39.0
52.9
29.0
33.6
40.6
BOARIKG FOUK.
Sead
"Mout h of Hunter's Creek . . .
Mom h of Difficolt Creek ...
Mouth of Castle Creek
Mouth of Fryine-Pan Creek
Mouth of Bock Creek
Mouth
Miles from
mouth.
64
55
48
43
25
12
0
Eleration.
Feet
11.676
9,4t0
8. '^41
7, 942
6.626
6,000
5,>734
Fall per
mile.
Feet
2:3
I61)
60
73
4d
28
GUNKISON UIVER.
Head
Mouth of Pass Creek
Head of upper caQon
Mouth of Slato River.
Mouth of Cochetopa Creek. .
At8tatlon71
At foot oren valley
Mouth or the White Earth. ..
Mouth of A creek
Mouth of /7 creek
Month Lake Fork
Mouth of Cebolla Creek
Month North Fork
Mouth of 6 creek
Month Uncompahgre River .
Mouth of Ronoldeau's Creek
Mouth
Miles from
mouth
200
185
176
157
141
13.5
130
123
116
114
112
97
62
50
45
40
Elevfttioo.
Feet
11, 176
0.869
0,570
a 176
7.725
7,':00
7,638
7. 4.'iO
7,:i50
7,327
7,213
6.^0
5,405
5, 220
5,100
4,925
4,523
FaU per
mile.
Feet.
153.8
32.6
73.7
28.2
4.2
12.4
26.9
14.3
11.5
57.0
27.5
39.9
14.9
25.2
35.0
10.0
JUNCTION OF STREAMS.
Eli'vntion.
Feet.
Mouth of Taylor River.-.l 8,300
Mouth of Deadman*8 Gnlch 9. GOO
Mouth of Cement Creek 8,500
Mouth of East Kiver 8,640
Mouth of Washin^irton Gulch 9,000
Month of Cascade Creek 8,970
Mouth of Dyke Creek 10,840
Month of Ohio Creek 7,775
Forks of Ohio Creek 8,400
Month of branch a of Smith's Fork 6,745
Month of branch b of Smith's Fork 7,500
Mouth of branch a of North Fork 5,500
Mouth of branch 5 of Coal Creek 7,077
Mouth of branch ^ of Rock Creek 6,000
Month of branch ( of Rock Creek 7,100
Month of branch 0 of Rock Creek 8,400
Month of branch /Plateau Creek 7,682
Mouth of branch y Plateau Creek 6,337
Month of br8.nch a Plateau Creek 5,680
28 H
TOPOGRAPHICAL REPORT OF NORTHERN DIVISION, 1874.
By Stort B. Ladd, M. £.
Washington, D. C, June 1, 1S76.
Sib : I have tlie honor to submit to you the topographical report of
the Dortheru division of the Uuited States Geological and Geographical
Survey of the Territories, to which I was assigned as topographer, for
the season of 1874.
The party, in charge of Mr. A. U. Marvine, geologist, left the ren-
dezvous camp, near Denver, on the 20th of July. A camp was made
for three days near Golden City, and a detailed survey made of the
country between Kalston Greek and Mount Morrison. We crossed the
Front or Colorado range by Berthoud^s Pass, and traversed the Middle
Park to our field of work north of the Middle Park.
The first station was made on the Ist of August, and the last one on
the 20th of November. The wagon-road from the White River Indian
agency to Rawlings Springs was taken, and Kawlings was reached on
the 28th of November, and Denver, by railroad, on the 30th.
Mr. Wm. S. Holman, jr., took the supplies for the party, and a mercu-
rial barometer to the White River agency, via Rawlings, and the
wagon-road from that point. The barometric station which he estab-
lished there is the base on which the majority of our altitudes depend.
The plan of the topographical work is exactly the same as used the
year before, and as aidopted by the other parties.
Very respectfully, yours,
STORT B. LADD.
Dr. P. V. HAYDieN,
United States Geologist^ in charge of the United States
Oeological and Geographical Survey of the Territories,
REPORT.
The country assigned to the northern division, to be surveyed during
the season of 1874, is north and east of the Middle Park, in Golorado.
The northern limit was north latitude 40<^ 30^ and the southern the
Eagle River from its source at the summit of the Mount Powell range
to its junction with the Grand River, and then the Grand. On the east
the work was to connect with that of the previous year on the western
and northern sides of the Middle Park, and to the west the work was
to be continued as far as the season would allow.
The most western point reached was nearly to longitude 108^, though
the average limit is about 107^ 45', This arrangement gave us a narrow
strip north of Middle Park, covering the southern end of the North
Park, of an average width of about eleven miles, and extending from
435
436 GEOLOGICAL SURVEY OF THE TERRITORIES.
the summit of the Front or Colorado range north of Long's Peak, west
to the Park range, which is tbe eastern limit of the bulk of our work,
and has a trend of north 25<^ west from Mount Powell. The dispo^itioD
of the country made it desirable to commence at the eastern end of the
!North Park district, and to extend the work to the west toward our
supply depot at the White Elver Indian agency, and when, early in
November, we reached the country between the Mount Powell range
and the headwaters of the Eagle, tbe storms and the clouds that hung
constantly around the mountains made it igipossible to continue tbe
work, and we were obliged to leave that portion for another season.
The total area surveyed is about four thousand one huudI^ed square
miles of mountain country^ interspersed with a few wide, open valleys.
The methods of working are the same as adopted by the oiher parties.
A line of primary triangulation stations bordering the country on th^
east and south and Dome Mountain near the center of the district, lati-
tude 40O 00' 57/'45, and longitude 10iO 04' 40."46, (approximate,) were
the points with which the secondary triangulation joining all the topo-
graphical stations were connected. Eighty-six principal stations were
made, together with some minor compass stations along the lines of
travel. The average distance of the stations apart was 6.84 miles.
A barometric station was established at the White Kiver Indian
agency, commencing on the 17th of August, and a meteorological record
has been kept from that time to date. Different members of the party
were observers while the party was in the field, and since then the
observations have been made by Mrs. E. H. Danforth.
A portion of the party was encamped at the mouth of the Engle
Eiver for twenty-six days, and a barometric record was kept there
during the time, which gives the elevation of that point very accurately.
The station at the agency is the base used in the calculation of the
m^ority of the heights ; for the work done while the smal) side-party
was at the mouth of the Eagle, that base was used as being much
nearer, and the work done in the Korth Park previous to the establish-
ment of the White Biver base depends upon the bases at Fairplay and
Denver.
The southern end of the Medicine Bow Mountains, which border the
North Park on the east, forms a high, precipitous, granite ran^e be-
tween the valley of the North Grand and the Park. East of the North
Grand rise the monntiiins of the great Front range, of the ^alne gene-
ral character as they are to the south, sharp, serrated summits, with am-
phitheaters on either side. The highest points of these ranges rise to
a little over 13,000 feet, but the general elevation is 12,500 feet. To
the north the Front range loses its rugged Alpine character and changes
to a high, heavily-timbered plateau range, separated from the Medicine
Bow by the Big Laramie iciver, and drained on the ea«t by the Cache
la Poudre. The tttuge in the other direction bears south 40^ east, and
culminates in the highest mountain of the whole northern districts
Long's Peak. The valley of the North Grand is narrow and close, ex-
cepting a portion of its lower course, where it widens into a broad
beaver meadow.
Grossing the Medicine Bow range, we descend by long, broken spurs
to the broad open prairie-like basin of the North Park, drained by the
North Platte River. Across the Park rises the Park range, a broad,
rounded mass, heavily timbered, about twelve miles in width, and with
an elevation of from 10,000 to 10,500 feet. The range retains this
character for fifty miles to the south, and then rises to the very rugged
precipitous range of Mount Powell. To the north, for ten miles, it re-
mains the same, and then changes to a more mountainous type, but not
i^ADD.j GEOGRAPHY GKNEBAL FEATURES. 437
as rough a one as to the south. The divide at the head of the Muddy
Creek of Middle Park is very low, but 8,772 feet elevation ; while at
BO point is the Park rangre lower than 9,000 feet, except where the
caiion of the Grand cuts through it. So, if this canon did not exist, the
entire drainage of the Middle Park would flow through the Muddy Pass
into the North Platte Eiver.
The main spurs or ridges between Park View Mountain and the Park
range, which, to the south Irom the divides between the Troublesome,
the west fork of the Troublesome, and the Muddy, have a northwest
and southeast trend parallel to the range.
Considering the country west of the Park range as a unit, the main
topographical feature is the White River plateau, a lava capped mesa,
irregular, and cut by deep canons and valleys, which olteu nearly sub-
divide it.
This western district comprises about three thousand five hun-
dred and twenty square miles, and the drainage is divided into three
systems, the Yampah or Bear Kiver, the White, and the Grand. The
Yampah drains nearly the northern half of the district, the White the
western central, about one-quarter, and the Grand the southern third.
The Yampah has a northeasterly and northerly course from its source
on the eastern side of the mesa, which, situated in the center, is a point
from which the drainage radiates, till it reaches the Park range within
a mile of our north line, when it makes a sharp bend and holds a course
due west till it joins the Green River.
The W^hite River drains the heart of the plateau, and the main stream
has its source in Trapper's Lake, which nestles in one of the deep-cut-
ting valle>s close under the clifls. The South Fork of the White, head-
ing near Shingled Mountain, cuis a deep precipitous caiion through the
center of the plateau.
The Grand River, which issues from the Middle Park through the
caiion in t^e Park range, flows through a broken series of gorges for
ninety miles, opening out occasionally into a small valley of from one to
five miles in length, but for the greater part of it« course in rough, often
impassable caiious. The Eagle flows through an open sage-brush val-
ley lor twelve miles and then through a narrow valley for five miles
before it joins the Grand.
From the White River plateau, the surface of which is irregularly
rolling, there rise a number of isolated mountains. Shingled Mountain,
station XLI, and point 17-XLI, from 500 to 1,000 feet elevation above
the general surface. These made excellent topographical stations. The
eastern edges of the spurs, as well as of the main plateau, are tbe high-
est, sloping on the west to the edges of the mesa, and falliog off on all
sides with abrupt, high clifl's, to the long, sloping spurs below. To tbe
east there are a number of ridges partially detached from the plateau,
and the highest points of these are the mountains that show so promi-
nently from the east, Dome Mountain and Mount Ornno, which stand
just south and north of tbe head of the Yampah, the highest mountains
west of the Park range in this district.
The Dome Mountain ridge is entirely separated from the [)lateau, and
the Mount Ornuo mass is connected by a narrow wall of rock, some-
what higher than the plateau at either end, in places but 3 feet in width,
and a sheer precipice on both sides of from 700 to 800 feet. To the
north lies the valley of the Williams Pork, a large tributary of the Yam-
pah ; to the south the headwaters of the Yampah itself. Standing near
the center of this wall, which is 125 feet in length, with outstretched
arms, and dropping a stone irom each hand simultaneously, they fall
for 100 feet before touching the sides of the clifl's. It was very much
438 GEOLOGICAL SURVEY OP THE TERRITOBIES.
cracked and sbattered, and another winter will probably denoiolisli this
natural causeway.
The eastern edges of the plateau and the main spurs and ridges bare
a northwest and southeast trend, parallel to the Park range.
West of the Park range and parallel with it is a broken range* abool
ten miles distant from the axis of the main one. Starting as a spar
from the Mount Powell mass it forms the high ridge of station LXXXI,
reaching to 11,000 feet. The Grand has cut a canon through the ridge,
leaving a detached mountain, station LXXX, north of the Grand.
Korth of station LXXX there is quite a low saddle ; then it rises again
to station LXXVIL To the north the Yampah has cut a small caiiim
through the range, but it tbere becomes lower, and soon falls off to the
broad, low ridge of station XV. West of this range, and between il
and the spurs from the plateau, lies Egeria Park, drained by the Yam-
pah, the Chimney Fork, a tributary of the Yampah, and Bayard Greek,
a branch of the Grand. It is an open, terraced basin, about twelve
miles long from northwest to southeast, and from one to four miles wide
The divide between the Yampah and Grand River waters is only a veij
low gravel terrace, scarcely noticeable.
The valley of the Yampah, between stations XVII and XV, forms a
small park about ten miles long and from one to three wide. Below
the great bend of the Yampah, near station XV, tor seven miles the
valley is a wide, open bottom ; it then closes into a caiion for nine miles,
and then widens out into another rich and fertile bottom, extending
almost continuously for eighteen miles down the river, and bordered oo
the north and south by low,- rolling hills. It is in this valley that the
new settlement of Uaydenville is started, the beginning being made in
November last.
Near the lower end of the bottom the wagon road from RawlingsP
Springs on the Union Pacific Railroad to the White River Indian agency
crosses the Yampah, and a small Indian trading-post, now kept by Mr.
Morgan, is located there.
The valley of the Yampah is the finest and roost promising of the
whole district. This river is bordereci by a growth of large cotton woods,
and the soil appears to be very tertile and productive. It has an eleva-
tion of from 0,200 to 0,800 feet. The only valley that rivals it in rhe
least is that of the White River at Simpson's Park, where the agency
is located; this, however, is on the Ute Indian reservation. Coal is
found in a number of localities along the Yampah, between it and the
White, as well as north of it, and although it has not been thoroughly
explored and tested, yet it promises to be very abundant and of good
quality, equal to any in the Territory-. The (Steamboat Springs are
located right at the bend of the Yampah, on both sides of the river, and
close to the bank on the north side. The water is lukewarm, of froQ
70^ to 720 temperature, and is strongly saturated with sulphur.
At the head of a small stream, a tributary of the Eagle, draining the
valley southwest of station LXXXII, there are a few quite small sul-
phur-springs, and on the banks of the Grand River, two miles below the
mouth of the Eagle, there is another set of sulphur-springs on both sides
of the river. A short distance below these springs there is a ver^' large
one that gushes forth close to the edge of the river, so that in the spring,
at high stages of the river, it is entirely submerged. This spring h;is
very little, if any, sulphur, though it probably has some salt, with possi-
bly some other ingredients.
North of the White River plateau the country is mountainous and
irregular, with no distinct, well-defined system.
The continuation of the spur, of which 6-XLI is the highest pointy
x-ii^D.) GEOGRAPHY — IROADS AND TRAILS. 439
^orms the dividing range between the White Eiver and the Williams
H^^ork and Waddle Creek tribntaries of the Yampah. It is a broad,
x^olling, heavily timbered range, with several prominent cone-sammits,
SLS Pagoda Peak and point 9-XXIX, and has three easy passes. An
old trail crosses between Pagoda Peak and the plateaa from the Wil-
liams Fork to the White ; a good trail crosses between Pagoda Peak
siDd point 9-XXIX from the main branch of the Williams Fork to the
"White, at an elevation of 8,300 feet, and the Government wagon-road
caresses through Yellow Jacket Pass, west of station XXXI, at an eleva-
tion of 7,493 feet
The plateao continnes to the sonthwest, forming the divide between
the White And the Grand Eivers, but it loses the distinctive mesa char-
acter to a great degree, and becomes more like a high, rolling range;
the streams flowing south cut deep, profound canons, while to the north
sloping spurs and hog-back ridges divide the tributaries of the White.
ROADS AND TRAILS.
There are two roads that penetrate this country, the Government
wagon-road from Rawliugs' Springs,on the Union Pacific Railroad, to the
White River Indian agency, and the one known as Berthond's Salt Lake
"wagon-road.
The first, starting from Rawlings' Springs, crosses the old stage-road
4bo Salt Lake City just west of Bridger's Pass, then following the valley
of the Muddy, crosses the Little Snake at the settlements, and, cross-
ing to Fortification Creek, follows that for most of its course, and fords
the Yampah River just below the mouth of Elk Head Creek and half a
mile east of Morgan's trading-post. It then follows a nearly straight
course, crossing the Williams Fork and the Waddle, through Yellow
Jacket Pass to the agency.
The second, which is a road surveyed by Capt. £. L. Berthoud, in
1861, from Golden City, Colo., to Provo City, in Utah, via Berthond's
Pass and the Hot Springs, in Middle Park, crosses the Park range at
Gore's Pass at an elevation of 9,590 feet; then through the small group
of meadows drained by Stampede Creek, across a low divide to Sarvis
Creek, and down that valley to the Yampah. For the last few miles it
leaves Sarvis Creek and follows down a small side-stream. Within a
few years, since the discovery of mines on the Elk and Snake Rivers, a
number of teams have been through by this route, and they have broken
a road from Stampede Creek through to Egeria Park, and that is now
the passable route, the former one down Sarvis Creek being but a trail.
Passing through Egeria Park and down the Yampah for seven miles,
it follows a nearly straight northwesterly course across to Oak <ind
Sage Creeks, then bearing to the west across a low divide east of sta-
tion XXIV to Skull Creek, and once more meets the Yampah, which it
follows down till it joins the Rawlins rocid. This is the route that is
now used, but Captain Berthoud's surveyed road divides on Sage Creek,
one branch passing up Sage Creek and across to the Williams Fork,
and the other leaving the present road at Skull Creek, passing up Skull
Creek to the Williams, where it joins the other branch, then across the
hills to the range east of Waddle Creek, where it joins the present road
to Simpson's Park and the agency. This portion of Berthoud's road
from long disuse has become nothing more than a trail.
From Simpson's Park the road follows down the White to the junc-
tion of the Green, then up the Uintah River and the Duchesne Fork,
and down the Timpanogos to Provo City, Utah.
440 GEOLOGICAL SURVEY OF THE TERRITORIES.
The country is traversed by a great many well-defined trails in all
directions. The principal ones across the Park View monntain-range,
from the Middle to the North Park, are through the Willow-Ci'eek Pass,
east of Park View, at an elevation of 9,683 leet, and one across the low
divide at the head of the Muddy Creek at an elevation of 8,772 feet
This is the pass crossed by Fremont, in 1844, on his return journey, and
he speaks of it as one of the most beautiful passes he had ever seen.
A fair trail crosses the Park range about live miles north of Babbit
Ears, » mountain near the Muddy Pass, capped with two sbarp points
of lava rock, to the valley of the Yampah, just above the great bend.
The most important trails in the western district besides thoBe men-
tioned in connection witb Berthoud's Bait Lake road are those leading
to and from tbe Indian agency. A large Indian trail to the Cochetopa
agency runs almost south from the White River agency, crossing the
Grand at the pionth of Divide Creek, thirty-seven miles below the
mouth of the Eagle, and then south up Divide Creek. A trail to the
mouth of Eagle Kiver follows up the White for five miles, then ascends
the rolling plateau and crosses it in nearly a straight line to the junc-
tion of the Eagle and Grand, passing down the long spur west of Caiion
Creek. The trail then follows up the Eagle River for twent^'-one miles,
and ascends the steep sides of the canon of the Eagle to the valley
southeast of station LXXI, the highest point between the Eagle and
the Grand. It crosses this valley and the ridge dividing it from the
Piney River, and passing along the steep mountain sides on the east of
the Piney and south of the Grand, it crosses the valley east of station
LXXXI and the Park range through a pass 7.5 miles south of tbe
canon of the Grand and just north of point 5 — XLI, and joins the Blue
River trail in Middle Park.
The greater part of the whole country is abundantly watered, and the
streams, with but few exceptions, are large and full. On the western
edge the country becomes drier and more barren, and soon merges into
the sterile, desolate region of Western Colorado. Longitude 108° is
about the eastern limit of the barren waste. The country to the west is
broken by low mountains, ridges, and terraces, but there are no com-
manding points, and away from the Yampah, White, and Grand Rivers
water is very rarely found. Careful measurements were made of the
Grand and Yampah Rivers so as to give the amount of water carried
by them. This is an important question in case the country ever be-
comes settled enough to require irrigation, in order to utilize for culti-
vation the dry plains, especially on the Blue and Muddy in the Middle
Park and along the Yampah, though there is no doubt that the sup-
ply is ample for any possible demand.
The Grand River was gauged at the hot springs, in Middle Park, on
July 31. The river at that point was 84 feet in width, with a small side
run 12 feet in width, and the greatest depth was 3 feet. The maximnm
velocity was 8 feet per second, and the amount of water 802 cubic feet
per second. Early in November the river was gauged again at a point
ninety miles below the springs, and just below tbe month of Eagle
River, but the Grand is so much smaller at that time, it being at its
minimum, that no direct comparison can be made between the tffo
results. ;
The Blue, the Muddy, and the Eagle add their waters to tbe Grand
between these two points, besides a great many smaller streams, yet the
river measured only 871 cubic feet of water per second. The small
amount is dne to the lateness of the season, the river being then at its
very lowest point. The width of the stream was 108 feet, the greatest
depth 3.7 feet, and the maximum velocity 3.4 leet i)er second.
I-ADO.I GEOORAPnY — ^ELEVATIONS. 441
Tbe Ynmpah was ganged in the middle of November, near the ford
"^^here the Bawllngs wagon-road crosses, and this result also gives tbe
minimnm amount of water in it at any season of the year. The width
wvLS 156 feet, the deepest pl^ce 2.5 feet, tbe maximum velocity 2.4 teet
per second, and the amount of water 364 cubic feet per second.
In the spring these rivers are very high and impassable until nearly
July, and the Grand i below the Blue is not fordable till August, and
tlieu only in a few phices.
Plenty of water is naturally accompanied by an abundant growth of
timber, and about one-half of the whole area is so covered, though a
^reat deal of it is small, and of no value as lumber.
The Park range is covered with good large timber, similar to the
front range, mostly pines, but with aspens and small low trees along
the lower edges. The Park View Mountain range and the Medicine Bow
are the same, the hillsides well covered with flat areas, jirms of the North
JPark, clear and open. These flat areas are covered with tbe lake deposits,
and wherever these basins exist, as in Egeria Park, and tbe parks along
"Yampah, they are free from timber, with the exception of the cotton-
T^oods bordering the streams.
The long sloping spurs from the White Eiver plateau and the heads
of the valleys draining it are well timbered, especially on slopes facing
the north.'
From the southeastern comer of the plateau, near station XLVII, and
the long ridge that, starting at this point, runs southwesterly from this
point around to tbe east and north to the month of tbe South Fork of
the White, and beyond it to station LV, the country is well, and in
places even heavily, timbered, coveringaboutTOOsquarerailes. Tbel)est
timber, pine and spruce, grows on the heads of tbe White, Wflliams
Fork, and Yampah Rivers, and on the top of the plafeau between Shin-
gled Mountain (station XLII) and station LIX. Tbe spruce-trees grow-
ing on tbe top, at an elevation of from 10,500 to 11,000 feet above the
sea, are large and flue, often reaching 3 feet in diameter.
A list is given of tbe elevations of the principal points and places.
A few are calculated trigonometrically and those are marked with a f,
and a few that are dependent upon an aneroid barometer are marked
with an a; the rest are all obtained from a mercurial barometer.
Lint of elevations.
MOUNTAINS.
Elevation,
feet.
Station T, Front range 12, 000
Station LX, (from '73,) ) i 12, 513
Station II > Medicine Bow range .. } 12, 761
Station V > ( f 13, 060
Park View, (from 73,) 12,433
Station VII .. 11^906
Rabbit Ears... ) (.... 10,710
Point 3-LXXIV, south of Gore's Pass . . [ Park range .. ^ .... HO, 620
Point5-XLlI ) (.... <11,240
Station LXXXI tll,26I
Station LXXl 11,336
Station LXXVII ^10,430
Station XVII 8,774
442 GEOLOQICAL SURVEY OP THE TERRITORIES.
WHITS RIVER PLATEAU.
ElevatioD,
feet
Station LII, northeastern edge f 11, 210
MountOrnuo tl2,lS)
Dome Mountain 12, 498
Mount Derby.... : tl2,253
Shingled Mountain, station XLII 12,072
. Point 2-XLII n2,276
Station XLVI, southern edge 11,367
Station XLI 12,030
Poiutl7-XLI m,957
Station LV 10,116
Pyramid Peak, station LI 1 1, Gil
Pagoda Peak 11,251
Point 9-XXIX til, 044
Station XXXI, east of Yellow Jacket Pass 9, 431
PASSES AND DIVIDES.
S3J £J is, 1 '^ «■» """I" <» «■« ''»'"■ P"". ! ; : l^.
Gore's Pass, Park range 9, 590
Divide south of station LXXXII, west of Piney Creek a 8, 422
Pass from Skull Creek to Williams Fork ... a 7, 797
Pass from main branch of Williams Fork to White River 8, 300
Yellow Jacket Pass a 7, 493
ELEVATIONS OF PARKS, VAXLBYS, ETC.
Valley of the jS^orth Grand 8,841
North Park, southeast corner ' 9, 053
North Park, southern edge 8, 596
Head of the Yanipah or Bear River 10, COO
Egeria Park, northern end 7, 500
Yampah Valley, near station XV 6, 781
Yampah Valley at Haydensville, mouth of Skull Creek * 6,382
Yampah Valley at Morgan's trading- post 6, 229
Valley of Sage Creek 6,948
Valley of Williams Fork, south of station XXVII 6, 047
Valley of the Waddle, foot of Yellow Jacket Pass 6, 654
Valley of the White, eleven miles above luouth of South Fork. 7, 592
Valley of the White at mouth of South Fork 6, 972
White River Indian agency 6, 491
South Fork of White, at lower end of canon 7, 551
Head of South Fork on plateau 10,9(K)
Lake on plateau below station LVIII 10, 337
Grand River, below caiion in Park Range 7, 000
Grand River, mouth of Hughes' Creek 6, 919
Grand River, near station LXIX 6, 618
Grand River, in valley one mile above Shingle Creek 6, 307
Grand River, mouth of Eagle River 6,116
Eagle River, at bend in caiion 6, 790
MEANS OF COMMUNICATION BETWEEN DENVER AND THE SAN
JUAN MINES.
By A. D. Wilson, Topographer directing.
Tfae Denver and Bio OraDde Railroad is now running daily trains to
Colorado Springs, Paeblo, and Gaiion City. Persons wishing to reach
the new mining district may take the train to either of the three previ-
ously mentioned places, and at these points they will have to provide
themselves with animals, except by way of Canon City. From this
place there was during last summer a regular line of stages running
to Saguache and Del Norte, but from these latter places there is not at
present any public conveyance. I mention the three points of starting,
as they are all more or less traveled.
Colorado (Springs is situated some seventy-six miles south of Denver
on the Denver and Bio Grande Baili'oad. Leaving the railroad at this
point, the traveler is obliged to procure his own conveyance, as there is
not at present any public conveyance from there to Saguache or Del
ICorte. The road from here leads by way of Manitou up the Fontaine
qui Bouille, crossing South Park at its southern end, passing by the
Salt- Works; thence down Trout Creek to the Arkansas Biver, which it
follows down some miles to the South Arkansas. At this point the road
joins with the one from Canon City, and then, following up Puncho
Creek, leads through a pass of the same name, to San Luis Valley, thence
skirting this valley along its western border to Saguache. This road
is somewhat longer than the others, but a very good and pleasant one to
travel, especially during the warmer portions of summer. The distance
by this route from Colorado Springs to Saguache 1 estimated at one
hundred and seventy miles.
The next route south is by way of Cafion City, This place is situated
on the north bank of the Arkansas Biver, near where it emerges from
the mountains, about one hundred and sixty miles from Denver by rail.
The road from Canon City passes around the first cation by keeping
some distance to the north of the river, then, swinging south, crosses the
river and again leaves it passing through the north end of Wet Mount-
ain Valley, where it again turns to the north and strikes the river in
Pleasant Valley 5 thence following up the river until it joins the Colo-
rado Springs road, where it crosses the South Arkansas. It is ab«>ut
one hundred and ten miles by this road from Canon City to Saguache.
Pueblo is situated also on the Arkansas Biver, about thirty-five miles
below Canon City, and one hundred and eighteen miles by rail from
Denver. The road leading out from this place crosses the plains
toward the southwest and strikes the Huerfano Biver at Badito. At
this point the road forks, one following up the river and crossing the
Sangre de Cristo range through the Mosca Pass, thence crossing the
San Luis Valley to Del Norte. The other branch of this road crosses
the river, and keeps farther to the south, crossing the range through
the Sangre de Cristo Pass, strikes the valley at Fort Garland, and cross-
ing from there to Del Norte. Both branches have to contend with the
443
444 GEOLOGICAL SUEVEY OP THE TERHIT0RIE8.
great sand-drifte wbicli bave accumalated on the eastern edge of the
San Luis Valley ; the one by way of Mosca Pnss being probably the
shortest by some miles, but at the same time having more sand to
contend with. With the exception of the sand, this is a very good road.
I estimated the distance from Pueblo to Del l^orte by Mosca Pa»8 to
be one hundred and twenty miles. I merely mention briefly these dif-
ferent roads to Saguache and Del Norte to give the traveler some idea
how to reach these 'points, as they are the last places of any note on
the way. Saguache is located on a small stream of the same name,
where it leaves the mountains and enters the San Luis Valley. The
enterprising citizens of this place have already gone to considerable
expense in building a wagon-road which is to connect this place with
tbe San Juan mines. But I fear it will take more labor and money to
make it a good road than tiiey at present can afford to expend on it.
This road is only approximately located on tbe accompanying map,
owing to its unfinished condition when we passed through that portion of
the country. The construction party was, when we passed them, August
12, nearly up to the junction of Godwin Creek and Lake Fork. The^ had
brought their supplies over the road in wagons, but there were many
)>1aces where mucb labor would be required to make it practicable for
heavily-loaded wagons. From this point on they will meet their great-
est obstacles. As I understood them, tbc^y intended following approx-
imately tbe course of tbe trail — that is, up Lake Fork. By this route
they can get a very good grade, but only with considerable ex^ieose,
until nearing the pass, where the mountains rise quite abruptly, and it
will be very difficult to construct a good road over this pass, as it is
quite steep on either side. This pass is 12,540 feet above sea-level.
Tbe trail over this pass strikes Animas River near its head, where
many silver-bearing lodes have already been located. From thii«
point it follows down the river to Howardville, a distance of about nine
miles, a portion of the way being over very steep and loose cf^&m sloiies,
over which it will be difficult to construct a road. The distance by this
road from Saguache to Howardville will be about one hundred and
thirty wiles. There is also a trail from Saguache, which is a much shorter
route for pack or riding animals than the road, but a small connecting-
link is wanting, which any one can easily supply by taking the accom-
panying map on which tbe trail is indicated.
From Los Pinos agency the trail follows up one of the branches of
Cochetopa Creek, thence crossing over to the White Earth, which it fol-
lows up until nearing the divide between it and the Rio Grande. Here it
turns to the south and descends to Antelope Park. Bnt the traveler
wishing to go to San Juan must keep <m in a westerly direction, and he
will soon strike a trail which leads him down to San Cristoval Lake,
where he will strike the Lake Fork trail, formerly described. The dis-
tance by this trail from Saguache to Howardville is about one hundred
and ten miles.
Del Norte is located on tbe southern bank of the Rio Grande, near the
foot- bills on the west side of San Luis valley, about thirty miles soath
of Saguache. This being the nearest place to the mines, it is from here
that the miners procui*e tbeir supplies at present. The wagon-road from
Del Norte follows up the river along its southern bank, meeting with no
obstacles of note until reaching Wagon- Wheel Gap. At this point, owing to
a loose slide, the owners of the road were compelled tochange it by bnildiog
a bridge over the river. This bridge was nearly complete when we passed
there. The road only crosses to recross again vei^ soon, and continaes on
the southern bank until nearing Bristol Head. Here it crosses to the
witso2f.l GEOGRAPHY — ^MEANS OP COMMUNICATION. 445
northern bank ; then, soon leaving the river, and skirting the foot of the
inountain, crosses a low spar, and descends to Antelope Park. This
point is about fifty-five miles from Del Norte. So far the road is very
good, having no heavy grades, and, passing as it does over the gravelly
bottoms, it is naturally solid and qaite smooth for a moan tain-road. At
this point the road again leaves the river, following up Crooked Creek
for about eight miles ; reaches a high pleateau, which it crosses, bear-
ing again toward the river ; descends a high and quite steep bluff; crosses
and recrosses the river, when it again leaves the river for a short dis-
tance, coming upon its bottoms once more at the Half-way House. So
far the road is passable for lightly loaded wagons ; but from hereon it
is of no use in its present condition, as it is about all they can do to get
an empty wagon over it. From the Half-way House the road follows up
the river for some distance, when it turns to the right, and ascends quite
a steep slope, winding its way along to the pass. It is at this point that
the greatest difiSiculty is met with, owing, first, to the sudden descent of
the slope from the pass to Baker's Park, the whole distance being some
fear miles, with a descent of 2,900 feet, and in the first two miles a de-
scent of about 2,300 feet ; and, secondly, owing to the very rocky and
bluffy charater of the slopes, it will be very difficult to give the road
swing enough to get anything like a good grade. Still this appears to
be the most practicable route at present, as there is a good road for so
much of the way.
The trail from Antelope Park does not follow the same course as the
road ; it more nearly follows the river, and crosses a pass about one mile
farther south, near the head of Cunningham Creek. This pass is a few
feet lower than the one through which the road goes. Height of trail-
pass above the sea-level, 12,090 feet.
The distance by the road from Del Norte to Howardville is about
ninety-five miles. There is a trail leading from Howardville down the
Animas; also another leading out to the northwest to the headwaters
of the San Miguel and Dolores. Both of these trails have been described
by Mr. Khoda.
The accompanying map gives the drainage in detail of the country
immediately surrounding the San Juan mines, with all the im()ortant
mountain-peaks, roads, 'trails, and other features of the country that
.could be represented within the limited time at my disposal. The lower
portion of the liio Grande was located preliminarily in order to show
the route of the wagon-road from Del Korte.
The heights of many of the important peaks and valleys are given on the
map ; and there will be a list giving the heights of all the higher peaks and
other important points, with an explanation of the method used in their
determination by Mr. Ehoda, who has worked them up with great care.
The small contour map of Baker's Park and vicinity will give an idea
of the character of the country which we were engaged in working up
the past season. It will also give some idea of the care with which this
region has been surveyed. Owing to the want of time, I was not able
to get more of the country drawn finally for this report.
Mr. Ehoda has written quite a detailed description of the country.
Therefore I will refer the reader to his chapter for any information that
may be sought in i^gard to the appearance or character of this region.
Dr. Endlich has also written a geological and miueralogical report of
the region surveyed.
446
GEOLOGICAL SURVEY OP THE TEBBIT0BIE8.
Fall of the Bio Grande from Cunnifigliam Paas to Del Norte, oommeneiug aipan.
To the moatb of Pole Creek.
Tbence to Lost Trail Creek .
Thence to Antelope P«i-k
Thonoe to Del Korte
Dittaaee.
JTOm.
8i
60
FUL
FseL
1.30O
l.WO
600
1,100
F^per
ML I
*
Fall of iAa Animaefrom, itivide letween it and east branch of Uneompo^fpre to the hncer rwi
of AnimoM Park,
To upper end of Baker'n Park
Tbeuce to lower end of park
Th«Qce to mouth of Cascade Creek.. .
Thence to head of Animan Pnrk
Thence to lower end of Animas Park
Distance.
jroes.
8
8
17
10
14
FaU.
FmL
8,000
SM
1,700
800
aoo
FaUpe
mila.
3»
as
100
ft
tL4
Fall of Lo8 Pinoefrom Wetninuche Pan, commencing at summit of
To point where tmil leaves stream
Thence to west branch
Thence to Valleoito Creek
Thenoe to Biff Bend
Distanoe.
MiU9.
ft
0
12
6
FaU.
FetL
7t3
1.S0O
1,000
400
FaU
■iiia.
1313
S13
FaU of VaUedio Creek from divide between it and Rio Grande, commencing at divide.
To janctlon of south branch
Thenoe to Los Pinos
Distance.
Fsa
ira0f.
5
21
FeeL
9,400
S,800
FaU per
Fall of Rio San Miguel, commendag at Bear Creek Pase.
To ralley below pass
Thence down stream
Do
Thence to Junction of east branch
Distanceh
JfilM.
8
4
9
6
FalL
9,400
600
800
1.100
F^lpcr
Bite.
4W
IAS
Fall of Unoompahgre from divide between it and Mineral Creek, commencing at iNcidie.
To small valley
To lower end
To lower end of oafion
To Junction of wcttt branch
Distant
JTOff
4
9
4
14
FalL
1.400
900
1.S00
1.000
Fdlpsr
S39
7L4
^wiuaoN.*
OEOOBAPHT — ^FALL OF STREAMS.
447
Fall of Lake Fork, oommendng at divide west of Bandie^s Peak,
To valley
Tlieoce tojanotion of aoath branch
Thence to month of Godwin Crock
Tbeuce to point where road strikes creek
Distance.
Fall.
MUet,
Feet
8i
3.S0O
H
1,S00
15
1,900
21
800
Fall per
mile.
Fat
880
SIS
80
3a9
Fall of Godwin Creek, commencing ai divide between it and Unoompahgre,
To Jnnctioo with north branch
Tlieoce to Lake Fork
Distance.
MUet.
74
10
Fall.
Feet
8.800
1,000
Fall per
mile.
Feet
374
100
COMPARISONS OF ANEROIDS WITH THE MERCURIAL BAROMETER.
The following table gives the comparisons of the aneroids with the
mercurial barometer at different altitudes, ranging from 5,000 to over
14y000 feet above sea-level. These comparisons were made very care-
fally, and as often as practicable, hoping thereby to have a good check
on any heights which were dependent on the aneroids; and at the same
time wishing to see if there was any regularity in the movements of the
aneroids. But there does not appear to be any regularity in the changes
which they undergo. Generally, in going up or down any considerable
height in a short time, the aneroids would not change fast enough;
therefore would make the difference between points too small, while at
the same time they always indicated too great an absolute height, always
reading less than the barometer.
In the tables given below, the readings of the barometer are reduced
to 32^ Fahrenheit. The aneroids are sup[H)sed to be compensated for
temi>erature.
The corrections to be applied to the aneroids are placed in separate
(lolumns, with the sign prefixed, which in this case is always plus, as the
aneroids constantly read lower than the barometer.
The instruments used were Green's cistern-barometer, and the small
watch-aneroids by the same maker.
Location.
Camp IS.
Camp 13.
Station 3
Station 3
Stations
Camp . . .
Station 6
station 7
Station's
Camp 80.
Camp S3.
Time.
3 p. m....
7 a. m....
3p.m
1 p. m . . . .
13. 49 p.m.
6 p. m . . . .
3 p. m . . . .
10 a.m....
3p. m
7 a. m . . . .
11. 50 a.m.
Date.
•Tnly
July
JToly
Jnly
Aug.
Aug.
Ang.
Aug.
Aug.
Ang.
Ang.
39,1874
30.1874
30, 1874
31, 1874
1, 1874
1.1874
3.1874
4,1874
0.1874
7,1874
7,1874
an
a
^if2
&
81.854
31. 717
18.633
10. 177
ttf.083
30.608
31.375
31. 753
1&934
83.134
31. 010
I
« .
31.13
1&10
1&60
18.40
19.83
30.48
31.00
18.34
31.37
sa7i
I
m
a
81.10
90.86
17.80
I
s
80.10
17.00
80.15
+ .784
.533
.577
.683
.788
.705
.753
.584
.864
.900
9
St?
e
+ .754
.857
.833
g
n
+ .000
1.617
1.633
1.400
448
GEOLOGICAL SURVEY OF THE TERRITORIES.
Looation.
Camp 31
Station 9
SUtiou 10
Camp 24
StatfoD 11
Camp 25
Cnmp26
Station 13
Camp 27
Station 14
Camp 28
Pass
ilniroas
Station 16
Camp 29
Paas
Camp 30
Camp 31
Camp 31
Camp 33
Station 31
Camp 33
Camp 34
Camp 36
Camp 38
Silverton
Camp 39
Station 29
Camp 41
Paaa
Camp 39
Camp 42
Station 30.......
Camp 43
San Miguel Lake
Camp 44
Camp 45
Station 33
Camp 46
Sution35
Camp 47
Station 37
Camp 46
Pa88
SutionSB
Camp 52
Camn.'>3
Camp 54
Station 40
Camp 55
Camp 55
Camp 56
Station 44
Camp 57
Camp 57
Station 47
Camp 58
Camp 59
Station 50
Camp60
Station 51
Station 53
Station 54
Station 58
Station 62
Station 63
Camp 73
By Station 64....
Camp 74
Time.
m
7 p. m . . .
8 a. m . . .
1 p. m . . .
9. ;J0 a. m
7 a. m
t2m
7 p. m...
7 n. m...
2 p. m . . .
7 n. m...
1 p. m. ..
7 a. m...
9 a. m . . .
2 p. m...
11.30 a. m
4. 30 p. m
11.30 a. m
6 a. m .
8 p. m.
7 a. m.
7 a. m.
1 p. m.
7 a. m.
7 a. m.
7 a. m.
7 p. m.
6 p. m.
6 p. m.
Sp. m.
6 a. m.
9.30 a.
1 p. m .
7 a. m.
2 p. m .
7 a. m.
13m...
4 p.m.
6 p. m.
2 p. m.
6 a. m.
2p. ro.
6 a. m.
1 p. m.
7a. ro.
2 p.m.
3 p. m .
6. 30 a. m
a 30 a. m
7 a. m . . .
13m
5 p. ra . . .
7 a. m . . .
7 a. m . . .
1 p. m . . .
6. 30 p. m
6. 30 a. m
4 p. m. . .
6. 30 a. m
6a. m...
13. 30 p. m
7 a. m...
10. 30 a. m
10a. m...
3.30p. m
12m
II a. m...
13. 20 p. m
7 a. m . . .
9 a. m . . .
6 p. m . . .
Date.
7,
8.
Ang.
Ang.
Ang. 10,
Aug. 11,
Ang. II,
Aug. 12,
Ang. 12,
Ang. 14,
Ang. 14,
Ang. }!>,
Aug. IS,
Ang. 16,
Aug. 16,
Aug. 16,
Ang. 17,
Ang. 17,
Aug. 18,
Aug. 19,
Aug. 19,
Aug. SO,
Aug. 22,
Ang. 23,
Aug. 2.3,
Ang. 24.
Aug. 28,
Aug. 29,
Aug. 31,
Kept. 2.
Sept.
Sept.
Sept
Sept
Sept.
Sept
Sept
Sept
Sept
Sept
Sept 10,
Sept 13,
Sept. 13,
Sept. 14.
Sept 15,
Sept 16,
Sept 19.
Sefit 30,
S«'pt 21,
Sept. 3-2,
Sept 23,
Sept 23,
Sept 2:).
Sept 24,
Sept. 26,
Sept 2(),
Sept 27,
Sept. 28,
Sept 28,
Sept 29.
Sept. 30,
Oct
Oct
Oct
Oct
Oct
Oct
Oct
Oct
Oct.
Oct
Oct
1
2.
6.
8,
9,
12,
15,
16.
".
17,
18.
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1814
1874
1K74
1874
1874
1874
1874
1874
1814
1H74
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1H74
1874
1874
1H74
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1J^74
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
1874
eft
IS
o ffi ^
too
^ S P
&
19. 667
18.U39
18.657
21.200
22. 133
20. 563
2i.coa
21. .^79
19. 017
20.876
18.213
20. 465
19.210
20, 262
1& 5.32
21. 207
19.4G1
19. 924
80.186
20.203
20.502
I a 343
20.514
19. 919
19. 906
21. .^94
21. 518
21. 307
la (Mi's
30.816
20.202
81. 345
2t 146
iai95
20.424
21. 132
21. 841
80.663
17.865
81.913
17. 815
20.397
19.008
30.686
20. 576
]a663
30.977
81.879
83.557
22. 116
23. C78
2:J. 725
23.452
22. :.03
23.927
24. 006
21. 856
23.123
22. 577
22.873
21.453
19.065
20.874
19.088
32.271
38.021
81.872
24. 854
23.046
34.633
8
c
« e
19.00
17.47
17.97
'31.* 18
19.70
20.73
20.60
laso
30.00
17.55
19. (K)
ia40
17.83
19.09
19.' 30
19. 60
"i9.38
19.01
19.04
80.54
20. 5U
20. 31
17.90
19.88
19.30
80.39
30.15
17.45
19.48
19.70
17.20
ii.io
'iai3
19.64
19..'50
17.85
19.90
20.73
82. 4:%
21. C9
88.70
'31.40
"n'oo
80.87
31 13
81.60
81.80
S0.4.i
IK'.a
19.90
la 85
81.80
20.95
20.83
23.31
22.60
83.62
o
o
a
o
o
.2
P4
ia7o
19.95
2t09
20.57
20.52
19.8a
19.33
If. 10
ia37
19.06
19.42
17.14
19. 32
laeo
la 73
30.10
19.61
19.07
30.10
19. 94
19.30
20.63
19.44
19.24
17.79
19.50
19.37
19.80
80.63
23.49
22.72
22.39
22.93
23.03
22.16
81.59
• • ■ - *
80.31
2.3.80
c
t
s
o .
c o
o
17.90
16.40
i9. 40
20.37
19.90
19.82
10. G5
]a68
17. 4«
ia30
19.40
17.76
ia20
ia45
ia46
ia73
16.53
lais
iao4
19.81
.9.56
19,' ii
ia47
19.54
19.43
ia56
19.17
19.04
la 85
20.08
16.01
18.64
17.80
laso
ia7i
19. 10
19.98
81.78
81,76
31. 95
31.66
■ ••••• I
32.18
38:35
21.49
2a 80
'19.76
«l9S
•
a
.067
.5t9
.687
.810
.702 !
.r03
.903
1.134
.909
. 866
1.018
.397
.788
.936
.903
1.055
.996
.745
.944
.963
.665
.715
"".'878'
1.046
1.016 t
.813 I
1.077
1. 149
1. 107 I
t026
1.085
1.103
1.006
a
^^
t ^«
I.
o
.967
I.2.'jO
1.04J
LIS!
i.o;»
9.'k3
.863
.96:1
.979
.717 i
.876 I 1.076
.663 I
. 773 1. 135
I.IIU
1.091
1.143
1.089
1.803
1.194
1.119
1. 176
1.207
1.806
1. 1:»
1.245
1.206
1.824
1.211
1.2S3
1.157
1.818
1. 186
1.206
1.177
1. 34 J
1.06T
1.005
1.0(^
.997
.9S6
.993
.977 t
1.07J I
L023 I
.974
.838
1.071
1.071 i
1.04-i !
1.044 I
1.046 I
L013 I
.963
.987
1.143
1.054
e2
« 3
s
1.69
L8»
1.7J8
1.7S
I.»S
i.9r
i.Tn
i.7di
1.73S
1.743
1.WI
I.S23
1.79
L7S4
L74;
1.166
1-73J
l.?4t5
1.716
1.8i»4
1.9G2
1.901
Lel3
1.933
1.773
L757
1.796
1.866
i<
1.8»
1.CJ7
1.918
1.775
1.1U
J.7fi
1.63i
1.133
1.777
1.603
L7U
'ITILSOK.]
DISCUSSION OP ANEROIDS.
449
Location.
Camp 1
Camp 8
Cainp 3
Caiup 4
Camp 5
Camp 6
Camp 8
Station 1
Camp
Camp
Camp
Camp
Camp
Camp
Camp
Camp
Camp
Camp »
Camp
Camp
Camp
Camp
Camp
Station 59
Station 67
Station 73
Station 76
Stations?
Camp
Station 89 .'
Station 90
Station 94
Station 05
Time.
6
6
6
6
7
6
6
0
7
6
1
6
7
5
7
6
5
7
5
7
6
6
7
6
6
7
12
9
9
U
6
7
5
2
to
3
p.m
a.m
p. m
a.m
p. ui
a.m
p. m
a.m
p.ro
a.m
p. m
p. m
p. m
a. m
p. m
a.m
a.m
p. m
a. ra
p^m
a. m
ro
m
m
m
m
P-
P-
a.
P-
p.
m.
a.m
a.m
a. m
p.ni
a.m
p.m
p. m
a.m
p. m
Date.
Jaly
July
July
July
Jnly
July
July
July
Jnly
July
July
July
July
July
July
July
July
July
July
Julv
July
Aug.
Aug.
Aug.
Aug.
Sept.
Sept.
Sept.
Sept.
Sept.
Sept.
Sept.
Sept.
Oct.
Oct.
3.1873
4, 1873
4, 1673
5,1873
5, 1871
6,1873
7, 1873
8,1873
8,1873
10, 187:i
10, 1873
10, 1873
11. ler?
14, 1873
14, 1873
16, 1873
17. 1673
17, 1b73
18, Ib73
19, If 73
21, 1873
22, 1873
3, 1873
5,1873
8,1873
11,1873
5, 1873
11,1873
14, lb73
17, 1813
25, 1873
26, lf7J
28, 1873
20, 187 J
2,1H73
2,1873
.J. c -
Ian
24.371
24.4%
22.251
23.254
2i.2C0
23.237
21. 181
21.035
21. 850
24. 347
21. 260
22.733
32.625
23. 515
23.288
23. 447
24.611
25.036
25.r69
23. 813
22.527
23.673
22.0L7
22.539
22.0:)8
30. 542
19. 706
21. 3*1 5
23. 689
21.232
22.006
22. 4J1
20. 50i»
21. 094
21.117
£2.280
«»
6
o .
a
a«j
ct*i
og
M .
CfO
srs
•'- .»■
12
•s o
ce M
Qi
9)
p;
P2
9
0
a .
e *
24.01
24.17
31.94
31.96
21. ! 0
81.05
20. ra
80.70
31. 43
18.41
16.25
17.70
17.55
18.14
17.90
18.10
10.21
19.60
19.61
17.30
17.10
17. 15 I
33.10
23.23
21.11
21.10
21.04
21.10
20.06
10.90
"22.08
20.07
31.40
31. 25
22. 13
21.89
23.08
23.14
33.62
23.68
21.55
21.29
26.' 50
21. 02
20.50
19.10
18.39
20.00
21. 10
19.99
20.57
SO. 91
19.18
19.70
19.75
20.76
Location.
i£5
a «*^
£38.
Camp -
81. 103
18. OO.'!
21. 072
20.812
18.322
20. 47
Station
Camn *....
^:::::::::::;:. .::..::::.::::::::::
Sution
Camp
I>o
20.003
18.190
21. 034
30.145
18. 570
20.134
10. 613
17. 934
20.986
20.020
17. 946
20.C64
10. 708
18. 127
20. 724
18. t)58
20. 572
20.283
18.114
20. r.e
10. 424
21. 749
ID. 400
Station
Camp
Do
Station '
Camp
Do
Station
Camp
Do
Station
Camp
Do
Station
Camp
8tUtK>Q
Camp
Do
Stition
Camp
Siatien
Camp .*
Station
20.04
18.43
80.90
20.73
18.18
20.525
10. 775
If. 00
£0.70
19.99
18.34
19.98
i7.79
20.65
19.775
17.74
19. 55
19.45
17.89
20.20
18.30
20.10
19. 89
17.775
19. 775
1&90
21. 33
19.08
80. .S9
18.80
20.50
20. :iO
17.80
30.11
80.36
17.50
30,33
1!). 45
17. 8T
19.44
18.96
17.18
20.85
19.30
17.28
19. 18
19.06
17.35
19.81
17.70
19.49
17.29
19. L'4
18.64
80.05
18.48
20. CO
80.66
20.53
20. 70
10.88
10.86
Garc'ner's
17.15
18.04
17.04
18.81
iaa7
17. 14
10.36
17.53
No. 3.
10. 9:»
18.03
.361
.326
.311
.294
.300
.287
.251
.335
.420
4.037
5.010
5.033
5^075
5.375
5.3e8
5.347
5.401
5. 436
5.458
5.513
5.487
5.523
6
p
2 •
|S
o
o
1.271
1.266
1.141
1. 1.~>4
1.160
1.137
1. 121
1.135
1.387
1.190
1.333
1.375
1.385
1.3r8
1.3<.7
1.471
1.416
1.3-8
1.263
1. i97
1.507
1.519
1.538
1. 442
1.376
1.375
1. :.to
1. '^42
l..'S26
1. 5il
1.329
1. :W4
1.367
1.529
Cont?ction tonne
roid, No. 4.
Correction toane
roid, 0.
■
a
e .
en
eo
.!»
0
.163
.513
.153
.175
.405
.125
ATi
.578
.173
.082
.518
.153
.142
..522
.637
. 197
■ .e-.s
.643
.213
.190
.:a4
.600
.804
.155
.695
.265
.230
.154
.700
.604
.874
.653
Oardoer iin.
.144
.754
.784
.336
.736
.639
• .244
1.089
.206
.666
.{'06
, .514
.8f<4
I.2.S4
.348
.TJ8
1.1C8
.237
.777
.0f7
. .024
.914
1 364
.358
.868
1.128
.472
No. 3.
. :.9J
.793
.333
.339
.824
.0214
.4i)l
.434
. 4':9
.836
.784
.389
1
:29 u
-)
REPORT ON THE TOPOGRAPHY OF THE SAN JUAN COUNTRY.
By Franklin Rhoda, Assistant Topographer.
In the following report I have adopted the very common system of
describing the country in the order of our travels through it. The
system is a very faulty one, but seemed to be the best possible under
the cireumstauces. In describing a river or a simple range of mount-
ains, the order of sequence is laid down in nature; all you have to
do is to commence at one end of the line and follow it. The mount-
ains in the so-called San Juan country, however, are very compli-
cated, and present no definite lines that may be followed in a descrip-
tion without leaving much uutold. They appear, not in a single range,
nor in a succession of ranges, but as a great mass. It was thought best
to intersperse here and there in the description of topography such
personal adventures of members of the party as might throw light on
any features of the country or its climate.
We started from Colorado Springs on the 14th of July, 1874, taking the
road leading up the Fontaine qui Bouille, and over Ute Pass iuto South
Park. It would have been much shorter to have gone to Pueblo by rail,
and thence on horse or mule- back around the southern end of the Green-
horn MouTitains, through Huerfano Park and Mosca Pass, and across
San Luis Valley to Del Norte. But at this time of the year we knew
that along the low plains the heat would be intense and the grass and
water scarce. As it was we had a delightfully cool trip all the way,
with plenty of grass for our animals. Our road lay across South Park,
thence down the Arkansas Eiver and across the range at Puncho Pass
into the San Luis Valley. We reached Saguache on the 24th of July, and
made inquiries of different persons as to the nature of the country for
which we were bound ; but although they were all deeply interested in the
prospects of the new mines, nobody could give us any definite information.
We could not even find out whether the country was made up of rugged
mountains or only high plateaus. Two days after leaving this place we
reached the Los Pinos agency, where the Southern Qtes receive such
supplies as are apportioned to them by the Government. This point
was in the extreme southwest corner of the district surveyed in 1873,
and was the point of beginning the past summer.
Our first station was made on a peak which had been occui)ied in
1873 as station 34. It is a low point, a few miles northwest of the
agency; and is less than 12,000 feet in elevation. Having a most beauti-
ful day, and plenty of time at our disposal, we found it very pleasant to
study the couutry that appeared in the southwest, in which our sum-
mer's work was to be. We could see none of the very rugged masses
of mountains which beset our path and taxed our energies in the months
following. What did appear to us was as follows: A little to the west
of south, and not more than fifteen miles distant, rose up the high group
in which station 33 of 1873 was situated, and containing several peaks
ranging in height from 13,500 to near 14,000 feet. Farther around to the
west, but much more distant, appeared a high pyramidal-shaped peak,
451
452 GEOLOGICAL SURVEY OP THE TERRITORIES.
which is situated sonth of the Eio Grande, and is marked on the map as
Kio Grande Pyramid. A little farther to the right, and still more dv$r
taut, was a double- topped peak, afterward occupied as station 23, and
named Mouut Oso. Still farther around, auother distant, high |)euk
appeared to be the culmiuation of a high mountain mass; this is Mount
^olus on the map. Nearly in the same direction, but much nearer,
there appeared a high plateau, extending over many degrees of the
horizon. Being more than twenty miles distant from us, and lying
wholly above timber-line, it was a very interesting feature in the land-
scape. At our distance it seemed to be covered with grass; but this we
afterward found was not the case. Our subsequent experience showed us
that in this part of the country these high super-timber-line plateaus ar«
very common. Immediately beyond this area was a high mass of red-
colored mountains, afterward the scene of some interesting electrical
experiences. A few miles northwest of this group Uncompahgre Mount-
ain appeared, presenting on its north side the peculiar precipice which
distinguishes it from all the surrounding peaks. North of this a series
of ri<lges and plateaus extends from the high mountains to the Gunnisou
Kiver.
Having made profile sketches of the mountains and drainage sketches
of the water-courses in the vicinity, and having taken angles to every
prominent peak, bluff, and stream junction visible, we started for camp.
The next morning found us on our way to the great San Juau country,
of which we had heard so much and found out so little. Our course at
first lay to the southwest, along the Ute trail, which leads from Los
Pinos over to the Kio Grande. We ascended one of the peaks in the
small group containing station 33 of the previous season, and had a
good view of the deep and rugged caiions leading outward from the
center of the mass. In the several succeeding days we made stations
3, 4, and 5 on the high plateau already mentioned. From this plateau
we got the grandest view of Uncompahgre obtained from any station
during the summer. The full height of the great precipice stood out in
clear profile. Its striking resemblance to the profile of the Matterhorn
gave us a wholesome dread of it, for as yet it had never been ascended
by any one, and we felt that to reach the summit might be beyond the
range of the possible. The plateau upon which we stood ranges in ele-
•vation from 12,400 to 12,700 feet above the sea, and covers an area of
about fifteen square miles. We rode over it on our mules, to make the
station, and found it covered with loose rock, which in some places was
so rough as to necessitate long detours in going from one point to
another. As in many other cases which occurred subsequently, ire
found this plateau covered with puddles of water, and wherever there
was soil it was always boggy. On the west and north sides it was ter-
minated by bluffs, rauging in height from 1,000 to 2,500 feet, the last
200 to 500 feet being nearly vertical. On the west side of the plateau
the bluff terminates below in rolUng, timbered land, which extends a
little over a mile to the bed of Lake Fork. The totul fall from the top
of the bluff to the stream is 4,000 feet, in a horizontal distance of one
and a half miles.
Having finished this part of the country, we traveled down the White
Earth to the point at which it emerges from the upper cafion. Here
the new road from Saguache crosses it at a small angle, and, swinging
far up to the north to avoid the high bluff's, it finally turns up Liike
Fork at a point about twelve miles from the crossing of the White
Earth. Thence our course lay up stream, and we traveled along }nst
west of our plateau stations and nearly under the bluff's. From a camp
RHODA.] GEOGRAPHY — SAN JUAN MOUNTAINS. 453
just below the junction of Godwin Creek and Lake Fork we mnde sta-
tion 8 on a point about five miles east of Dneompabfyre I*eak. Tho next
station to be made wa^ on tbe great peak itself. In order to accomplish
this, it became necessary to move with our pack-train about five miles
up Godwin Greek, to a point where it is joined by a small stream com-
ing in from the north. Leaving the train at this point, and taking an
extra mule with us to carry our blankets and food, we rode with great
difficulty np the side gulch, and camped at an elevation of 11,900 feet,
near the timber-line. We started out early the next morning, expecting
to have a very difficult climb. We were terribly taken aback, however,
when, at an elevation of over 13,000 feet, a she grizzly, with her two
cubs, came rushing past us from the top of the peak. Contrary to all
expectations, we found the ascent very eas.y,and arrived on the summit
nt 7.30 a. m., hsiving been two hours and a half in climbing np 2,400 feet.
We found that l:he bears aforesaid had been all over the summit of the
peak, though how they got up over one or two short but steep passages
iu the ascent, puzzled us not a little. The summit of the mountain is
quite smooth, and slopes from the brink of the great pi-ecipice toward
the south. It is composed of several successive Hows of lava, in hori-
zontal position, which gives it a stratified appearance, and causes the
slope to the south to appear terraced in profile. On the north the edge
is sharp and definite, and the precipice so perfectly vertical, that by
dropping a stone a few feet from the edge it lell 1,000 feet before strik-
ing an obstacle,, as we determined by timing the descent. The bluff
surrounds the peak on all sides except the narrow strip on the south end,
and is about the same height all around, but not so nearly vertical as
on the north side.
From here, for the first time, we were able to see the great massive
ness of the mountains iu our district. To the south the peaks appeared
in great numbers, and in the <listauce appeared a group of very scraggy
mountains, about which the clouds were circling, as if it was their home.
Subsequently we found that they were most of the time thus enveloped.
The high mountains near us covered the horizon from the east around
by the south to tbe west. Nearly due west of us appeared a very high,
sharp peak, which was afterward ascended as Mount Snefiels, and just
to the south of it another high mass, bearing iii its center a large, flaring
patch of snow. The culminating point of this was, later,«tation 35, or
Mount Wilson. Southeast of us, and about eight or ten miles distant,
was a mass of peaks, filling the whole space between Lake Fork and
Godwin Creek, all of a bright red color. The highest of these points is
over 14,000 feet above the sea. Ten or fifteen miles to the southwest
was another smaller mass of lower peaks of the same color, while in
various places appeared mountains of white, yellow, and blue, all the
colors being very well defined and clear They were caused by the oxi-
dization of iron and other ingredients of the rocks. To the north the
mountains fall very suddenly down to the bed of the Gunnison ; in fact,
the peak is situated on the extreme north line of the Uucompahgre
Mountains. Just before we left the summit, clouds came along, qnd we
were soon enveloped. It was at this time that we expi rienced, for the
first time in the season, the electrical phenomena which later intorfered
so much with the topographical work. As at this time these phenom-
ena were not very marked, and as our experience on all the peaks was
very similar, the detailed account of them is reserved tor another place.
^Ve made the entire descent that evening from the summit to Godwin
Creek, where the packtrain had left us, getting the benefit of a rain be-
fore reaching camp. Up to the second day before this the weather had
454 GEOLOGICAL SURVEY OF THE TEEBITORIES.
been very fine, but from this time till fall, rain commenced early evefy
afternoon, and continued into the night Moving up Godwin Creek.
Dr. Eudlich made a special examination of some of the highly -colored
peaks aheady mentioned, while Wilson and I rode up to the head of the
cauon and out upon a high and pretty extensive plateau, which extends
from a hijuh, sharp pinnacle a few miles west of Uncompahgre Peak
around tlie heads of (Godwin Creek and Lake Fork to the head of the
Animas. It forms the divide between these three streams and the Un-
compahgre River. An area of fifteen or twenty square miles is alwvc
tlie timber-line. Ten or fifteen square miles have an elevation of over
12,000 feet. The timber line here ranges from 11,500 to 11,900 feet
• above tlie sea. This w^hole area is covered with a very short growth of
grass, which is almost entirely unfit for feed for animals. This is com-
mon with all the grass growing high up on the mountains; it is not nn-
tritious. Unlike the plateau east of Lake Fork, this is not snrroonded
by bluffs-. Instead of being smooth and nearly level, like the former, it
is rolling and cut up by gulches. The sloi>es down to the surrounding
streams are steep, but bluffs are very nire. The ground is not very
rocky, but like all the soil at this elevation, is very damp an<l bogg^'. A
number of small lakes are dotted here and there over it, and in many
places springs of ice-cold water gush out from the rocky prominences,
fed by the banks of eternal snow which are scattered about in considw-
able numbers. In crossing this elevated region a strong west wind was
blowing, and, the temperature being below the freezing-point, riding was
very disagreeable both for our beasts and ourselves. Under these cir-
cumstances we were not so observant as w^e should otherwise have been.
Still, there were so many new and interesting things about us that we
could not fail to notice some of them.
The eastern half of the plateau drains out through a canon leading
northward and westward into the Uncompahgre Kiver. We crosse<l its
bead on our tramp, and noticed that it fell very suddenly, till within
about two miles of us it became a deep, narrow canon, at which point
the stream turned abniptly to the west. From this fact we were en.v
bled to get a good broadside view of the north bluff of the canon, and
we saw it weathered out most curiously, being worn into almost all cou-
cei\able fantastic shapes, the general appearance being that of a great
wall covered with niches and statuary. Time would not permit us to
go closer and' make h more careful examination ; so we had to content
ourselves with a distant view. From the headwaters of this creek we
crossed a divide running laterally across the i>lateau, and for some dis-
tance the drainage was into Godwin Creek, until, near the peak upon
which we made our station, the water again flowed to the north. From
station 10 the canon of the Uncompahgre Kiver appeared in all its rug-
gedness. From here we got a fine view of Mount Sneftels and its sur-
roundings. We could see no possibility of ascending the peak from the
east side, as it was cut up by rugged canons and innumerable bluffs aud
pinnacles ; these latter ornamenting all the ridges leading down from
the great peak and its near neighbors.
In some i)laces numbers of the pinnacles massed behind one another
presented the appearance of church-spires, only built after a much grand-
er style of architecture than most of our modern religions edifices, in
some places two systems of vertical pillars w^ere separated by a narrow
strip of horizontal lava- flow, and served to heighten the fantastic appear-
ance of the rock-forms. The fact that we stood on a peak four or five
miles distant from the scene described, will give some idea of the great
size of these pinnacle forms. A month later we had another muchnearer
BHODA.I GEOGRAPHY SAN JUAN MOUNTAINS. 4ft 5
and finer view of this same curious group from a peak several miles
southwest of us. Beyond this we saw nothing of interest that eanuDt
be better described in the sequel.
The next day found us retracing our steps down Godwin Creek.
After can)i)ing a night at the junction, we moved up Lake Fork, making a
station bv the way on a low point near the stream. A few miles above
the junction we came to a beautiful lake bearing on Mr. Front's map the
name "San Cristoval." This is by far the finest of the many little lakes
we saw during the summer. It is in the bed of the canon, and has been
formed by a slide from»the east side of the stream. Judging from the
growth of X)ines over this slide we concluded that it had taken place in
very recent times, but how recent we could not determine. The lake is
about one mile and a half in length, and in some places as much as a
cjnarter of a mile in width. Several very small islets covered with
willows add much to the beauty of the scene. A thick growth of pine
timber surrounds it on all sides. To the east there is a tolerably easy
slope back to the foot of the bluffs of the high plateau. On the west
side the high mass of red mountains rises abruptly from the water's edge.
It was near the lower end of this lake that the Randolph party of
artists discovered the bodies of five men the day after we passed them
at this i)oint. They are supposed to have been murdered by white men
for their money. The canon of Lake Fork is nowhere so rough as that
of Godwin Creek, and the trail is quite good for the greater part of the
distance to the head of the stream. After camping a short distance
above the lake, and getting a good night's rest, we took an early start
on one of the most curiously interesting and strangely dangerous trips
of the season. We had to ride up the creek several miles before making
the ascent of the peak for which we were traveling. From this fact we
were thrown late and got ciiught on the summit in one of the afternoon
storms. Intermingled with other unusual drawbacks, we had a fair share
of the common but not less disagreeable climbing over loose rocks and
through fallen timber; neither were events of the chase wanting to add
to the great variety of incidents encountered during this eventful day.
The object in view was to make a station on the highest point of the red
mass above mentioned. In order to accomplish this, wo had to follow up
a ridge, along which patches of loose rock alternating with tinjber made
the riding very difficult. It soon became impossible to follow the ridge
any farther, and we had to cross the gorge on our left, going down 300
or 400 feet, and up again more than a thousand feet to the sumuiit of
the next ridge. liiding was out of the question, so we had to lead our
mules. After getting out of the canon the ground became smoother,
and near the timber-line we rode along without difficulty, the land being
very open and covered with grass. It was here that a considerable herd
of mountain-sheep appeared in the distance. We saw them before tliey
saw us, and, leading our mules out of sight, slipped through the timber
with the utmost care; but before we could get in position the sentinel
of the herd, posted on a prominent point, gave the alarm, and they all
instantly took to flight. Wilson succeeded in shooting one on the run.
As we had had no fresh meat for two weeks, the result of the shot was
very gratifying to us all.
For the rest of the ride the ground was covered with a short growth
of grass, but devoid of trees, as we had passed the timber-line. At an
elevation of 13,000 feet the soil ended abruptly, and from that point on,
all was loose rock. Here we hitched our mules to stones, and, taking
the note-books and instruments, continued the ascent on foot. This part
of our work was quite easy, although the height we had to climb wiis
456 GEOLOGICAL SURVEY OF THE TEERIT0EIE8.
nearly a thousand feet vertical. Before reaching the sammit of the first
high point on the ridge, we noticed stray clouds wandering ap and down
the neighboring canons, as if only waiting for us to reach the top betm
commencing the attack.
Seeii]g that it would be imi>os8ible to reach the main peak before the
storm would burst upon us, we made our station on the first point. The
maiu peak is 41 feet higher and a mile and a half distant, being connected
wiih it by a long unbroken ridge. Had time permitted, we should prob-
ably have occui)iod both points as stations, but we were unfortunately
prevented from doing this by the peculiar circumstances to be described.
Station 12, the southern and lower of these two points, is situated in the
upi)er bend of Lake Fork, where, from flowing in a southeasterly direc-
tion, it swings around to the east. Near the base of the peak Lake Fork
receives its principal tributary from the south side, which on Mr. Proul 8
map bears the name of Snare Creek. This peak is the most southerly
of tlie red group included between Godwin Creek and Lake Fork. Its
lieif>ht is J3,9(>7 feet above the sea. On the north and feast sides the
slopes are quite steep but regular, while on the south and west the sides
are very precipitous, with a fall from the summit to the valley below of
4,400 feet in a horizontal distance of one mile.
On arriving at the summit, Mr. Wilson hastily made a rough sketch
of the surrounding drainage, and then set up the instrument, while I
proceeded to make a profile sketch of the mountains south and west of
us. VVe had scarcely got started to work when we both began to feel a
peculiar tickling sensation along the roots of our hair, just at the edge
of our hats, caused by the electricity in the air. At first this sensation
was only perceptible and not at all troublesome; still its strength sur-
prised us, since the cloud causing it was yet several miles distant to the
southwest of us. In the early part of the storm the tension of the
electricity increased quite slowly, as indicatifd by the eflfect on oar
hair. By holding up our hands above our heads a tickling sound
was produced, which was still louder if we held a hammer or other
instrument in our hand. Tbe tickling sensation above mentioned in-
creased quite regularly at first, and presently was accompanie I by a
peculiar sound almost exactly like that produced by the frying of bacon.
This latter phenomenon, when continued for any length of time, becomes
highly monotonous and disagreeable. Although the clouds were yet
distant, we saw that they were fast spreading and already veiled many
degrees of the horizon. As they approached nearer, the tension of the
electricity increased more rapidly, and the extent of our horizon obscured
by them increased in nearly the same ratio; so that the rapid increase
in the electric tension marked also an increased velocity in recortling
angles and making sketches. We felt that we could not stop, tbougb
the frying of our hair became louder and more disagreeable, for certain
parts of the drainage of this region could not be seen from any other
peak, and we did not want to ascend this one a second time.
As the force of the electricity increased, and the rate of increase
became greater and greater, the instruireut on the tripod began to
click like a telegraph-machine when it is made to work rapidly; at
the same time we noticed that the pencils in our fingers made a simi-
lar but finer sound whenever we let them lie back so as to touch tbe
flesh of the hand between the thumb and forefinger. This sound is at
first nothing but a continuous series of clicks, distinctly separable
one from the other, but the intervals becoming less and less, till finallj
a musical sound results. The eflect on our hair became more aad
more marked, till, ten or flfteen minutes after its first appearance, there
RHODA.] GEOGRAPHY — ELECTRICAL PHENOMENA. 457
was sodden and instantaneous relief, as if all the electricity bad In^en
suddenly drawn from us. After the lapse of a few seconds the cause
became apparent, as a peal of thunder reached our ears. The light-
ning had struck a neighboring peak, and the electricity in the air had
been discharged. Almost before the. sound reached us the tickling
and frying in our hair began again, and the same series of phenomena
were repeated, but in quicker succession, at the same time the sounds
becoming louder. The clouds now began to settle into tbe Great
Canon of the Lake Fork, and boiled about in a curious manner; here
and there a patch of cloud would separate from the main mass and
move about by itself. In passing over a thick cluster of pines down
near the bed of the canon, the lower parts would get caught and drag
through with the greatest seeming diflBculty. Tbe different parts seemed
to be affected by different currents in the air, and at times two little
masses of cloud would pass each other less than a mile apart, but would
soon turn aside, or rise up, or lose themselves in the great Cloud that
pretty nearly'filled the Great Oaiion and its branches. At times a
portion of the mass, moved by an upward current, would rise several
hundred feet above the general level, and, the force ceasing, would top-
ple over and slowly fall back and lose itself in the general mass. The
whole moved about m a chaotic manner, producing a curious effect.
When you consider that the top of the cloud was not less than 2,000 feet
below us, you can form some idea of the strange scene that presented itself
to our eyes in those exciting times. Tbe clouds soon begaii. to rise up
and approach us. As they did so, the electricity became stronger and
stronger, till another stroke of lightning afforded instantaneous relief:
but now the relief was only for an instant, and the tension increased
faster and faster till the next stroke. By this time the work was getting
exciting. We were electrified, and our notes were taken and recorded
with lightning speed, in keeping with the terrible tension of the storm-
cloud^s electricity. The cloud reached us, coming on like a fog, looking
thin and light near us, but densely white at a short distance. All the
phenomena before mentioned increased in force a'ter ea<5h succeeding
stroke of lightning, while the intervals between strokes became less and
less. When we raised our hats our hair stood on end, the sharp points
of the hundreds of stones about us each emitted a continuous sound,
while the instrument outsang everything else, and even at this high
elevation could be heard distinctly at th<^ distance of fifty yards. Tbe
points of the angular stones being of different degrees of sharpness,
each produced a sound [>ecnliar to itself. The general effect of all was
as if a heavy breeze were blowing across tbe mountain. Tbe air was
quite still, so that the wind could have played* no part in this strange
natural concert, nor was the intervention of a mythological Orpheus
necessary to give to these trachytic stones a voice. Having completed
a rough sketch of as much of the sarrounding country as was not ob-
scured by clouds. I hastily took up the mercurial barometer, hoping to
get a reading before we should be compelled to leave tbe summit ; but,
alas! too late lor success. The lightning-strokes were now coming thicker
and faster, being separated by not more than two or three minutes of
time, and we knew that our peak would soon be struck. As I took tbe ba-
rometer out of its leather case, and held it vertically, a terrible humming
commenced from the brass ring at the end, and increased in loudness so
rapidly that I considered it best to crawl hastily down the side of the
peak to a point a few feet below the top, where, by lying low between
the rocks, I could return the instrument to its case with comparative
safety. At the same time Wilson was driven from his instrument, and
458 GEOLOGICAL SURVEY OF THE TERRITORIES.
we both crouched down amoDg the rocks to await the relief to be given
by the next stroke, which, for aught we knew, might strike the instru-
ment which now stood alone on the summit. At this time it was pro-
ducing a terrible humming, which, with the noises, emitted by the
thousands of angular blocks of 3tone, and the sounds produced by oar
hair, made such a din that we could scarcely think. The fast-increasing
electricity was suddenly discharged, as we had anticipated, by another
stroke of lightning, which, luckily for us, struck a point some distance
away. The instant he felt the relief, Wilson made a siidden dash for the
instrument, on his hands and knees, seized the legs of the tripod, and
flinging the instrument over his shoulder dashed back. Although all
this occupied only a few seconds, the tension was so great that be re-
ceived a strong electric shock, accompanied by a pain as if a sharii-
pointed instrument had pierced his shoulder, where the trii>od came in
contact with it. In his haste he dropped the small brass cap which
protected the object-glass ot the telescope; but, as the excitement and
danger had now grown so great, he did not trouble himself to go back
after it, and it still remains there in place of the monument we coald
not build to testify to the strange experiences on this our station 1±
We started as fast as we could walk over the loose rock, down the
southeast side'of the peak, but had scarcely got more than 30 teet from
the top when it was struck. We had only just missed it, and felt thank-
ful for our narrow escape.
We could not follow down the ridge we came up, as, in the prei^ent
state of affairs, it was highly dangerous to cross any prominent |>oiut,
even though it should be much lower than the i)eak itself. Ilail and
sleet began to fall freely, and as we de8cende<l to a lower level ihev
were exchanged for rain, with which we were well drenched, even before
reaching the mules.
We found Dr. Endlich waiting for us, having just returned from the
ascent of a lower point of the main peak, where he had experienoeti
similar phenomena to those already described, only dififeriug from them
in degree. He said he had seen the lightning strike our peak, and at
first thought that we might have been caught, till finally he saw us
coming down the mountain.
Our mules seemed glad to see us, not because they cared one straw
for us personally, but because our arrival was the signal for the retara
to camp. Whether they had been pestered by the electricity, we could
not tell, but they were doubled up into the most compact shape that
mules are capable of assuming, and did not seem to appreciate at all the
romance connected with a cold rain-storm at a high altitude.
Hastily putting on the saddles, we started down the mountain-side.
By this time the clouds enveloped us entirely, and rain fell almost with-
out intermission till long after we reached camp.
On our way we loaded one of the mules with the meat of the sheep
killed on our way up, but as it was a very difiicnlt npatter to tie the
whole animal securely across the saddle, it gave us a great deal of
trouble, as in going down steep places it would slip forward, and in
going through brush it would be pulled back. To go back the way we
came, was such a very difficult task that Wilson concluded to take a
short cut for camp, though this involved the risk of coming to bluflfs or
impassable slides. We had to lead our mtiles the whole way, which w«is
very steep, and composed of loose reck mixed in among the thin, straight
stems ot the quaking-asp trees. Here and there we came to lai^
patches of loose d^is without any^trees, and were compelled to fall
»HODA.] GEOGRAPHY CAMP INCIDENTS. 459
l)ack and take a new tack. The rain was still falling heavily whenAhe
sun set and darkness commenced.
In these high altitudes there is scarcely any twilight, and darkness
quickly follows sunset. I will not go through all the details of our
descent, as nothing occurred beyond what hus happened in the experi-
ence of every mountain-climber. We reached camp late in the night,
thoroughly drenched, and had to eat supper in the rain, which was any-
thing but pleasant.
If I could end the history of the adventures of this remarkable day
by describing how we were pleasantly housed in dry, comfortable quar-
ters, and how we contentedly '* wrapped the drapery of our couch about
us and lay down to pleasant dreams,^! would. But, alas ! how the ro-
mance would be taken out of the story if 1 should tell hovt we crawled
iuto our low, short, and narrow little tents, with the water running
under at the edges, and leaking through at the top, and how we had to
lie as still as possible lest we might disturb the pools of water gradually
collecting on our blankets, and precipitate them into the inner recesses
of our bed clothes. All this and more shall I leave untold, and cease
to disturb the several members of the party, placidly snoring away in
the bal>e-like innocence of their slumbers. And while they thus replen-
ish their wasted energies with the nocturnal balm of sleep, may the un-
wearied mind of the reader wander like a restless ghost up and down
this interesting caiion, and observe with care the high and picturesque
walls of trachyte which extend from the creek-bed to the summit of
ever- memorable station 12, and wonder, it may be, at the pine-trees scat-
tered here and there in the cracks in the rock, 2,000 feet above him,
having scarce a root-hold, and looking so diminutive as to suggest the
idea that some Japanese had been there and applied their wonderful
urt to §tunt them to their apparent pigmy stature. If, too, he extends
Lis observations up the scarcely less imposing caiion of Snare Creek,
ho will find many more things wonderful in their nature, but too varied
to tind a phtce in such a hasty sketch as this. If the reader, after hav-
ing satiated his curiosity with the many wonders of nature here laid out
before him, will return from his wanderings to the camp he left the night
before, an interesting scene will soon present itself to his eyes. If, a
little before the break of day, he observe closely the tents of the sev-
eral sleepers before mentioned, he will soon observe a movement in the
one occupied by our huge black cook. That little circumstance marks
the dawn of the next fiscal day, even though the first object emerging
from the tent be as black as night. In all countries it is a recognized
fact that the darkest part of the night comes just before the dawn, and
the present case tends to confirm the truth of the adage. The morn-
ing is bright and clear, but all things not under close cover are wet,
and wood is no exception to the rule. The cook searches about under
trees and bushes till he has collected together an armful of tolerably
dry branches, and then makes the fire. The fire burns, and another era
in the cook's exigence has commence<l. He takes four sheet-iron pots,
all of different sizes, and starts for the creek. A man of less muscle
would content himself with uvo. He soon returns with all the vessels
filled with water, and places some of them on the coals to heat, one for
the coffee, the others for cracked wheat, hominy, or other articles. At
this stage of the proceedings there is some commotion in another tenr,
and presently the two packers emerge from their cover fully equipped
lor the day. One immediately starts out to hunt up the mules, while
the other puts the packs and aparejos in order. The cook proceeds to
bake his bread in a Dutch oven, while the rest of the party still snoi-e
460 GEOLOGICAL SURVEY QF THE TEREIT0RIE8.
ou. In tbe intervals of bis cooking be opens tbe me>s8-boxe8, sets tbeni
about four feet apart, opens out tbe leaves, and, placing a support un-
der tbe middle, spreads bis clotb, and tbe table is ready. A short time
before everytbing is ready be rings the first bell for breakfast, by yell-
ing out, in tbe barbarous mountain dialect, '^ Grub pileP or sometimes
simply '^ grub," for sbort. At tbis tbere is great commotion, and the
rest of tbe crew ^' pile out " in all i^^orts of sbapes and in all states of
nudity. Tbey burry, for tbere is no driver like hunger, and they noir
feel a yearning in tbe inner man that Ciinnot be repressed, and their
love of sleep itself gives way. A general rush for the nearest water
soon takes place. In a few seconds all are washed, and immediately
commence tbe attack on tbe breakfast- table. Thev make short work of
it, and at 7 o^clock all are in their saddles and off.
Following tbe trail np tbe creek, we found it very rough, but at a
point west of station 12 the bed of tbe canon widened out, and from
tbere our riding was quite easy. Leaving a notice on a tree near tbis
place, for the train to encani]), we ascended a low peak to the south and
west of tbe creek. From tbis point we succeeded in clearing up some
])oii)ts in the topography which bad been unavoidably missed from sta-
tion 12. Two miles west of it was a very higb, massive mountain, with
a great horizontal baud of white running across the face of a high
bluff' on tbe northeast side of the peak. Tbis mountain bears en the
map tbe name of Handie's Peak, and was ascended the day after this
as station 14.
From station 13 we had a splendid view of the red mass to the north
and east, station 12 being the nearest of all tbe x>eaks. The last 2,000
feet in height was composed wholly of dull-red dSbris^ with very few
bluffs. Here appeared some of the finest mountain forms any of.us had
ever seen. From our distance, whicb was several miles, the ind'ividual
stones were all lost to tbe eye, and tbe slopes appeared as if they were
made of red sand, but of course having the forms which naturally result
from coarse debris. The tops of the ridges were nowhere jagged, but
were invariably formed of gracefully-flowing curves, while mountain-
lines could scarcely be more beautiful than tbe magnificent sweeps of
tbe curves formed by tbe long debris slides. Except on the south and
west sides of station 12, these curves were nowhere broken by any con-
siderable bluff's. Having readied tbis station early in tbe morning, we
were not troubled with storms during our work.
Several large silver-bearing veins crossing tbe ridge near this station
gave us the- first intimation of onr approach to the mining region. We
descended to camp, which we found just at the base of the i>eak,
and arrived quite early in the afternoon. Tbe next day, August 14,
we moved up stream, leaving directions with tbe packers where to make
camp. We rode up a small creek coming in from tbe south, which
drains tbe basiu between station 13 and Handie's Peak. Tbe ground
most of tbe way was very miry, and tbe brush and timber very difficult
to pass through. After passing the timber-line, the only difficulties in
our way were tbe boggy ground and rocks. One or two very steep
slopes, along whicb we bad to ride, were very disagreeable ; but much
less so for us than for tbe poor donkeys. At an elevation of nearly
13,000 feet we found a grassy patch of ground, which was large enough
and level enough for our mules to stand on without much danger. Hav-
ing secured them to the rocks, we climbed up the peak, which we found
a very easy matter, as tbe total lise was scarcely a thousand feet and
tbe slope quite gentle. A short distance below tbis summit, at an eleva-
tion of about 13,500 feet, we found some shallow prospect-holes sunk
BHODA.] GEOGRAPHY SAN JUAN MOUNTAJNS. 461
Oil a vein which cat transversely across the ridge. As yet we had seen
none of the miners, but these holes, with accompanying notices writ-
ten on a stake, indicated their presence somewhere in the vicinity. We
soon leacbed thesninmitof Handie's peak, and found it not near so
acute as most mountain-suramits in this region. This peak is very
massive, with high bluffs on the east side, which continue along the east
ridge around to station 13. Between the two stations is a deep basin,
amphitheatrical in form. To the south and west the slopes are steep, but
not precipitous.
To the west, and several thousand feet below us, we saw several little
lakes of a bright emerald-green color. We had no opportunity to make
any investigations as to the cause of the color, but from observations
later in the season we concluded it must be due to vegetation at the bot-
tom of the lakes. The white band already mentioned as appearing on
the east bluff was found to be coniprsed of volcanic ash. Here, again,
we saw a band of sheep, but having left our guns at the mules we could
not shoot them.
Early in the day we noticed the clouds hovering about the quartzite
peaks, as we had seen them so often before. They never completely
veiled all the peaks of the group, but early each day began to circle
about them in a restless sort of a way, like so many mighty lions about
their lair. To us this apparent restlessness suggested a consciousness
of their terrific destructive power, which only awaited a mandate from
the ** God of storms" to be set in motion. We even now held those
peaks in awe, as there seemed to be established somewhere in their
midst a regular "manufactory of storms." Our subsequent experience
among them never completely obliterated this idea. About 1 o'clock
in the afternoon the clouds again came on, accompanied by hail and elec-
tric phenomena similar to that previously described. We could detect
the electricity in the. air long before the clouds reached us by holding
our hands high in the air, when a faint clicking was audible.
The phenomena were precisely similar to those experienced on station
12, but having reached the summit earlier in the present ca«e, we were
able to leave before it became very dangerous. Just before leaving
the top I slung the strap of the tripod over my shoulder, and experi-
enced a sharp pain at the two points where the tripod touched me.
Otherwise the phenomena were much the same as on the previous sta-
tion. This peak is 13,907 feet above the sea, and 30 feet above station
12. Alter the hail and rain commenced, and fell incessantly till far into
the night. The following day we crossed the pass from the head of
Lake Fork to the Animas. The elevation of this pass is 12,640 feet.
The ground up to that point is very boggy and the riding disagrex^able.
The rise in the last mile of distance is more than 1,000 feet. How
the people of Saguache ever expect to bring a wagon-road up this
I cannot see. On account of the surrounding bluffs there is very little
opportunity to wind the road up it, while the miry nature of the soil
will require vast sums of money to be spent after the grade is obtained
before the road can be made passable. The fall from the pass down to
the Three Forks of the Animas is very sudden. Leaving the train to
proceed to Ilowardville, wherever that might be, we climbed up a peak
on the north side of the trail. This point commands the headwaters
of the Animas, and is 13,675 feet in height. We succeeded in getting
a few of the most necessary details of the typography, but as we had
traveled a considerable distance since morning, it was late before we
reached the summit, and about the usual time the electric storms again
commenced. By this time the romance C(>nnected with these pheuom-
462 GEOLOGICAL SURVEY OF THE TERRITORIES,
ena had all disappeared ; and at tliis time and thereafter, whenever
our hair began to fry, we generally disappeared at pretty short notice.
We never waited again so long as we had done on station 12. As we
were working on the peak, peculiar sounds reached our ears from the
depths of the Animas Canon, 2,500 (eet below. They resembled very
much the whistle of a locomotive when heard from a great distance.
By listening carefully and looking through our glasses, we formed a
shrewd surmise that this strange sound was the last indrawn note of the
plaintive bray of the jackasses used by the miners in bringing the ore
down from the mines. The harsh lower notes had all been dissipated
before they reached us, leaving nothing but the refined essence of the
sound behind. We considered this as a conclusive evidence of ttie pres-
ence of white men, and immediately descended to our mules. The trail
down to the Animas was quite steep, notwithstanding it wound arouod
a great deal. For the last part of the distance the fall w^as very suddeo
down to the Three Forks. The total fall from the pass is 1,400 feet
in two miles. At what is called the Three Forks, or the junction of the
three creeks which form the head of the Animas, we found several cabins
with a number of miners about, who kindly showed us specimens of ore
from their various mines. As Dr. Endlich will give a detailed description
of the mines, 1 will refer the reader to his accompanying report. A
very short distance below the forks, the great bluffs of the Animas
Canon commence, at first more or less broken up by slides and by gorges
formed by streams from the mountains. A little while after leaving the
forks the trail crosses the Animas, and follows across the great ix>ck-
slides which come down to the water's edge on the east side of the
stream. These extend many hundred feet above the trail, and are ter-
minated above by a series of high bluff^ij, one receding behind the other
and separated usually by small debrin slides, siuular to the great one
below: sometimes very steep grassy slopes form the connection between
the bluff's. Above all, a long slope, more or less steep, <x)nnects the last
and highest with the mountain-peaks above, which are from 3,000to 4,0(iO
feet above the stream-bed, but seldom ever visible from the trail, as the
near precipices cut off' the view. The bluffs on the west side are for
a long distance much less broken than on the east, and instead of having
slopes at their bases, rise abruptly from the bed of the canon, in many
places a thousand feet, nearly vertical. But the series of perfectly inac-
cessible bluff's often rise from 2,000 to 3,000 feet above the stream, and
are connected with the mountain-peaks by steep grassy or rocky slopes.
In some places the bluff's form the abrupt termination of what from
above are seen to be sharp, rocky ridges, leading down from the peaks.
In the upper end of the caiion I he only gorge cut through the western
wall is that of Eureka Gulch. Near its junction with the Animas this
is very narrow, but a short distance back it widens out into a considera-
ble basin. A very interesting thing in connection with these bluffs is
the fact that many little streams run over the top and reach the bed of
the canon by a succession of little falls. These give a picturesque appear-
ance to these otherwise bare bluff's. Still more important is their hear-
ing on questions connected with the working <»f the mines. A fall of
from 1,000 to 2,000 feet could be easily obtained. It can scarcely he
doubted that there is a never-failing hydraulic power continued in tliese
little streams sufficient to work all the machinery that can ever he
brought into these mines. All that is required is to apply it proi>eily.
In making this general assertion, 1 do not refer simply to those streams
which fall over the bluff's of the main canon of the Animas, tor it must
be remembered that, up Cunningham, Arastra, and other gulches, there
RHODA.1 GEOGRAPHY BAKER's PARK. 463
are bundreds of other similar streams that can be usi^d just as well, if
Dot even better than these.
While crossing the great slide on the trail, we could see miners at
work against the blufPs on the west side of the river. Curious-looking
zigzag trails led up to these mines. Others were tunneling from the
bed of the stream, and seemed to be in a poor position in case of a great
spring-thaw, as all their work would then be wasted. At one place we
saw an ice-bridge over the stream, which struck us as a novelty, for the
middle of August, at an elevation of ouly 10,000 feet, in this latitude.
At a point about five miles below the Three Forks the steep slide across
which we were riding abruptly euded, and we came out into a thick
clump of trees in which were several log cabins, bearing on a flaring
sigu-boiird the word " Eureka," evidently intended for the name of a
town that was expected to be, though what had been found here to sug-
gest the name was not immediately apparent. It is not impossible,
however, that the first settler coming up the Animas here found his far-
ther upward progress barred by the great rock-slide. At this point the
bed of the caiion suddenly widens out to a quarter of a mile or more in
breadth, forming the upper end of Baker's Park. A great portion of
the level ground is here covered by willows and swale grass, cut through
and through by old beaver-ditches. After leaving Eureka, the ground
is very uneven, and quite devoid of timber, except up the sides of the
caiion.
The bluffs on the west side become more and more precipitous, and
less broken up by gorges; while on the east the few bluffs which pre-
sented themselves farther up stream are exchanged for steep rocky
mountain-slopes, with few bluff's. At a point about three miles below
Eureka the Animas is joined by Cunningham Creek, a considerable
tributary, coming in from the east side. Howardville, containing at the
l)reseut time some eighteen or twenty log cabins, is situated on both
sides of this stream near its mouth. This is the first settlement in
Baker's Park, and among its other attractions can boast of a store, a
butcher-shop, assay oflQce, shoemaker shop, and post-office. Although
as yet there is no regular mail-communication with the outside world,
it is expected that a regular mail-route will soon be established by the
Post-Office Department. All mail is now brought in from Del Norte by
occasional travelers, and letters cost ten cents besides the regular United
States postage.
From this position a splendid view of some of the silver- veins can
be obtained. The face of the high bluff's, west of the town and across
the river, is covered with a net- work of yellow veins, extending from
the bed of the stream up as far as we could see. Later we found that
these same veins cropped out on the other side of the mountain, indi-
vidual veins being continuous the wtiole distance. We found some of
them crossing the highest point of the ridge at an elevation of 13,500
feet, thus giving a vertical depth for the outcrop of 3,800 feet, while the
horizontal distance was not less than the thickuess of the ridge, a
length of from three to four miles. How much farther they may have
extended horizontally, we could not make out in our limited time.
At a point nearly west of Howardville the bluff's end, and steep grassy
and rocky slopes take their place and continue to the lower end of the
park.
On August 16, the day after our arrival at the town, we crossed the river
and ascended a peak northwest of Ilow^ardville, but not quite visible
from that place on account of the intervening bluffs. The slopes were
all grassy, but so steep that we could ride but a small part oi the dis-
464 GEOLOGICAL SURVEY OF THE TERRITORIES.
tance. Wo came npon the top of the ridge near u little sharp point on
the spar, which I believe is the one designated by the name of '' King
Solomon's Mountain." Just a little below the top of this point we fooDd
a level patch of ground about 20 feet square, where we concluded to
leave our mules, as such level places seemed to be rare in this vicinity.
Looking about, we saw only one stone of sufficient size to hitch oar ani-
mals to, and that was an oval one; but as no alternative presented
itself, we tied the ropes of the two mules together, and then fastened
them as well as we could to the stone. The result of this will be seen
on our return.
The main peak was about half a mile to the north of us, but as the
ridge was easy to walk over, we had little difficulty in reaching the top.
On this peak we made station 16. Its elevation is 13,54L feet, as deter-
mined from the mean of twenty -three readings with a mercurial barom-
eter. This point is not very sharp, but is simply the culminating point
of several rocky ridges. From herea splendid view of the vicinity of Ba-
ker's Park may be obtained, although only a small part of the park
itself is visible. In order to understand rightly the situation and pecu-
liar position of this very interesting park, it will be necessary to give now
a general description of it, leaving the minor details to be filled in in onr
future travels. From this point we can see nearly the whole of the great
depression of which Baker's Park forms the most important part. Just
to the east of us the Animas runs along, its deep canon nearly 4,000 feet
below our present position, but the high bluffs bordering on the west
succeed in completely hiding the stream from view. Howard ville is also
shut out from the sight by the same obstruction, although it almost
comes within the field of view. The fall from the summit of this peak to
the stream near Howardville is 4,001) feet in 9,500 horizontal. Just
across the river, Galena Mountain has a fall to the Animas of 3,700 in a
horizontal distance of 7,000 feet, while down to the nearest point on
Cunningham Creek, the fall is 3,500 feet in 5,000 feet honzontal. On the
southwest side of Cunningham Gulch the fall is even greater than this.
These cases are not unusual specimens, but I have selected them becanse
the i>eaks are well known and can be easily found on the map. I could
instance many others where the fall was full as great and even greater.
From station 16 we had a good view up Cunningham Gulch, from the
fact that the continuation of the direction of the stream passed almost
exactly through the station.
Along the east side of the Animas a line of high peaks extends, from
its head down to the lower end of the great c;inon, a distance of thirty
miles. At the north end of the line, but draining into Lake Fork, is
Handie's Peak, with an elevation of 13,997 feet. Next come two name-
less peaks, the first having an elevation of 13,830 feet and the second
13,770 feet above the sea; then Galena Mountain, with an elevation of
13,290 feet, and next. Mount Kendall, 13,380 feet above sea-level. Be-
low this for some distance lower points continue the chain, till we come
to the group of quartzite peaks, ranging in height from 13,000 to 14,0r4
feet, wbere the line culminates in Mount iEolus and Pidgeon's Peak,
and, falling off suddenly to the south, soon loses itself in the plains of
Southern Colorado and New Mexico. The great and important feature of
this region is the far famed Baker's Park. Small in area and quite nn-
important in itself, it would be utterly disregarded if situated in other
parts of Colorado; but, located as it is, surrounded on all aides by the
most rugged mountains in the Territory, if not in the whole Rocky
Mountain system, this little area of flat land becomes an object of curi-
osity and interest. When looked at as the center of the great mining
ODA.] GEOGRAPHY — BAKEE'S PARK. 465
cllstrict, it becomes an object of great-practical importance. But not till
one has crossed over the several passes leading out of it can he feel a
13 roper regard for this little spot, so carefully guarded by nature from
t^be invasion of man. In itself, it is nothing more than the bed of the
deep cu&on of the Animas, spread out at the lower end to a width of a
xnile or two. It extends from the little town of Eureka, already men-
-fcioned, down the Animas to the base of Sultan Mountain, a distance of
Cbbout nine miles. It is divided into two parts, the upper of which is
oontained between Eureka and Howardville, a distance of about three
miles, and is quite rolling, so much so as to be scarcely worthy, the
name of park. Below Howardville the caiion again contracts till within
about three miles of the base of Sultan Mountain, when the cauonbed
^widens out into a beautiful level piece of land, about three miles long,
in the direction of the stream, and having a width of from one to two
niiles. It contains, in all, from 2,000 to 3,000 acres. This is the true
Saker's Park ; but the division between the two portions, as we have
described them, is not important, and in nature not well defined. The
^wide part above Howardville tapers almost insensibly into the narrow
part below it, but the line between this narrow part and the true park
below is quite definite. «
The new town of Silverton, at present containing about a dozen houses,
is situated near the center of the level area, on the south side of Cement
Creek, a stream flowing into the Animas from the west, and passing
through the park. Bounding Baker's Park on the south is Mineral
Greek, which, flowing from the west, highly impregnated with iron, sul-
phur, and other ingredients, hugs closely the foot of Sultan Mount-
ain, and joins the Animas near the entrance of the lower or Great Canon.
Almost all the water in this country is as pure as any in Colorado, but
this stream is so strongly impregnated with mineral ingredients as to
be quite unfit for drinking. The elevation of Silverton is 9,400, and of
Howardville 9,700 feet. From our present position, looking down the
valley, it seems to be completely closed up by Sultan Mountain, and the
exit of the river is iiot visible. At the lower end of the park the Ani-
ihas swings around toward the southeast, and for about seventeen miles
cuts a most terrific canon, ranging in depth from 2,000 to 4,500 feet in
depth, through quartzite rock almost as hard as steel. It might have
been expected that in the beginning the stream would have selected its
course somewhere near the junction of the trachyte and sandstone with
the quartzite. It se^ms, however, to have been turned by some agency
another v/ay, and so cut its course through the harder rock this long
distance, without being at any point more than three miles distant from
the softer material.
In order to get a true conception of the isolation of Baker's Park from
the rest of the world, a thorough understanding of the passes leading
out of it is necessary. First, let me say that the ruggedness of the
Great Caiion below the park is such that travel through it must long be a
matter of great difficulty, though it is said that some miners have passed
up from the plains on the south into Baker's Park by that route. The
trail at present most traveled by persons passing between Baker's and
Animas Parks crosses over the southeast slope of Sultan Mountain. At
the divide this trail has an elevation of 10,460 feet, but the highest point
is several bundled feet higher than this. This route is the roughest and
most dangerous of any leading out of the park, and even in the best
summer weather is unsafe for pack or riding animals.
The next pass is tbe one on the southwest side of Sultan Mountain,
which has an elevation of 11,570 feet above the sea, and, though not
30 H
466 GEOLOOtCAL SURVEY OF THE TERRITORIES,
dangerous like the preceding^ is very disagreeable, from the bogs, falks
limber, and rock-slides which beset one's way. Another Is ibe Bear
Greek Pass, leading firom the head of Bear Creek to the head of tbe
San Miguel, on the west side of the mountains. Its elevation is 12,696
feet. On the east a long stretch of fallen timber in a hogj throngii
which the trail passes, makes travel very difficult. On the west a gresit
rock-slide, over which the trail leads, is scarcely less disagreeable.
Two passes lead over to the head of the Uncompahgre Biver, but, a^
the box-caiion of the latter bars all egress, they require no description
here. To the east of our present position are the two passes at present
mostly used by persons passing to and from the mines. The first, from
the head of Lake Fork to the bead of the Animas, having an elevation
of 12,540 feet, has been alrendy described. The other, the pass from
Cunningham Gulch to the Bio Grande, has an elevation of 12.900 feet
at the highest point of the trail. Over this has passed almost every-
thing that has been brought into the park. The trail is very steep,
and in the best weather is muddy, and after a rain it becomes perfectly
horrible. When it is remembered that the height of a great part of tlvp
park is only 9,400 feet, it will be seen thAt the usceut from the valley
to each of the five passes at present used will l)e, in teet^ as follows:
1,300, 2,200, 3,200, 3,140, and 2,690. This gives some idea of the way
this little valley is isolated from the outside world. This, then, is the
far-famed park, named otter that daring leader of his little band, who
lost his life within its bounds. This is the cul de sac into which he and
his men were mercilessly driven by the Indians in 1862. How many
fell in the massacre, how many starved or froze to death, seems even
yet to be veiled in mystery. But how the present survivors ever escape<l
might well remain a mystery when we consider the great depth of
snow that must then have covered these high mountain-passes, and
that, at that date, the country was perfectly unknown. From our
station 16 only the lower end of the park, including Silverton, is visible.
The view of the mountains, however, is very extensive, all the high
oeak stations made up to this time being plainly visible, except the
irst one south of Los Finos agency. Mount Sneffels stands out boldly,
ibout fifteen miles to the northwest of us, while about an equal distance
o the east of us appears the high peak, called, from its shape and loca-
ion, the Eio Grande Pyramid. Just a little east of south the quartzitc
)eaks again stood out in their peculiar ruggedness. From this i>oint
»ve also h£id a good view of Arastra Gulch. Its upper end is a rocky
imphitheater, between 12,000 and 13,000 feet in elevation. In it^ center
was a little lake. At the lower end of the amphitheater there is a very
ibrnpt fall of from 1,000 to 2,000 feefc down to the bed of the creek.
Having reached the summit of this peak unusually early, we bad
)lenty of time to study the topography carefully. Just as we were fin-
shiug up the work of the station, and had commenced building a small
nouumeut out of the few stones in the vicinity, the well-known tickling
sensation about the roots of our hair again commenced, and we could
;ee its cause in the shape of a heavy rain-cloud which was slowly drift-
ug up the canon. We could see long dark streaks extending from the
iloud to the valley below, indicating heavy rain. All rainstorms in
his country, when seen from a distance, present this appearance. A
toutinuous mist-like connection extends from the cloud to the eartb,
jut through this are streaks much blacker than the rest. To a person
macquainted with those storms, these streaks would appear as bands
.>f vapor, a little thicker than the rest. In truth, however, the part that
seems like thin mist is heavy rain, while the black streaks are almost
ODA] GEOGEAPHY — MOUNTAIN CLIMBING. 467
tinbrokeD streams of water. These are what are nsu'ill^'^ known in tbe
moantaius as water-sponts. Wo left tbe snmmit before the electricity
became very tronblesome, bnt tbe rain which followed we could not
avoid. Packing up oar books and instruments, we walked down to the
place where the males ought to have been, bat where, to onr amaze-
tnent, they were not. Looking over the ridge, we saw the mules, still
bitched together, standing on the steep east slope, about forty yards
from the summit, bnt the round stone was nowhere to be seen. A heavy
farrow through the snow-bank, near tbe top of the ridge, with several
deep indentations in the soil below, told a carious tale.* It seems that as
tbe storm came on, a strong.cold wind arose from the west, which, with
tbe accompanying rain, made the mules feel very uncomfortable, as
they were on the west side of the ridge. In order to better themselves,
they moved over to the other side, slowly dragging the stone after them,
till, renehing the brink, tbe steep slope animated the otherwise inert
stone with a considerable power, and it in- turn took the mules in tow.
l>f course, as soon as they foand themselves pulled they drew back,
but, finding tbe stone inexorable, one of them moved up a step and
found herself relieved of tbe strain, and commence<l nibbling the short
^rass to be found in this vicinity. But what one gains the other loses.
The whole weight of the stone now pulls on the second mule; but it is not
iu the nature of tbe beast to resist for a long time a steady and unre-
laxing strain when unaccompanied by swearing. Bhe moves a step forward,
and, finding relief, goes to grazing. Thefirst by this timehas forgotten all
about the stone, and, finding herself suddenly jerked, her whole asinine
obstinacy is aroused, and she braces herself for resistance, but after
a minute or so, finding the pulling force unalteced, and hearing no oaths
proceed from the stone, she slowly comes to the conclusion that this is
Dot a human contrivance, and moves up. Thus by slow degrees the
stone pulls them down the slope, over the little snow-bank and some
distance beyond, disputing, of course, each step of the way, for such,
alas I have we too often found, to our sorrow, to be the nature of the
beast. After reaching a short distance from tbe top of the ridge, the
rope evidently slipped off the stone, and the latter, rolling faster and
faster, could have found no obstruction to its course for fall 3,000 feet
down the mountain. What tbe mules themselves thought of their mys-
terious leader they never revealed ; nor did we wait long in the cold
rain to bear their story, but hurriedly patting on the saddles, dragsred
them down that mountain much faster than the stone did ; but they
moved on joyfully, for they knew as well as we that they were going to
camp and to gra«s. Their shriveled fohrms and backs, curve<l up when
we first found them, indicated clearly the fact that they were disgusted
with the country, especially all of it above 13,000 feef in elevation.
Tbe rain now fell in torrents, and the grass being thoroughly wet, the
walking was very disagreeable, but tbe slope was very steep and riding
on oar tired beasts very slow, so we walked most of the way and dragged
our mules after us. Reaching Howardville, Mr. Wilson found that the
expected supplies had not arrived, so he concluded to finish the piece of
country east of Howardville and down the Bio Grande as far as might
be convenient. The next day, August 18, we started eastward up Cuu-
niogbam Gulch, up which a well-marked trail leads over to the Rio
Grande. This is by far the most interesting of the secondary cailous of
the Animas system. After passing the main bend, which is about two
miles east of Howardville, the side-slopes become steeper and steeper,
and finally end altogether in becoming nearly vertical bluffs. These are
nearly, if not quite, as high as those along the upper course of the Ani-
468 GEOLOQICAL 8UBVEY OF THE TERRITORIES.
Dias, already described. On the west side, these bluffs are rather more
precipitous thau ou the east, and come down closer to the stream-bed.
These consist usaally of a series of bluffs one above the other, receding
from the view. Over the last tier, which is from 1,000 to 2,000 feet above
the stream, numeroQs small streams of water pour, and passiDg over
the sacceeding bldffs in falls nnd cascades present a beautiful spectacle.
In the early spring, when the snow is melting and they are swollen to
considerable streams, the sight must be magnificent. A namber of
mines are located high up the slopes wherever they are not too steep to
be ascended. Here and there a little low hut is visible on the east
slope. Near the head of the galch. the trail i» very muddy and badly
cut up by travel. The upper part of the ciiuou ends abruptly wiiL
steei), high bluffs ou all sides, except the- narrow strip up which the
trail winds to the pass. Several lodes are located at the head of the
gulch. The amphitheatrical form of the head of the caiiqn with the
great bluffs are very characteristic of volcanic formations, and all over
the SSan Juan region they are the rule rather than the exception. Nev-
ertheless, the sudden termination here of the great Cunningham Gulch
is exceedingly interesting. The stream falling over these bluffs serves
to heighten the effect.
The trail now leaves the creek and ascends the east slope. It is very
steep and always muddy and slippery. The grade may be appreciated
by calling to mind the fact that from the bed of the stream to the pass
the rise is about 1,500 feet in one and a half miles horizontal.
The incessant travel over this trail by the miners, with their horses,
mules, and burros, keeps it ip a bad condition. Although it can scarcely
he said to be dangerouSv still its slipperiness adds much to the labor of
the already overwrought beasts of the miners. The really bad part ot the
trail is only a small part of the .whole distance. Ou the summit the
ground is gently rolling, and the trail parses betweeu low hills which
form the principal part of the country in the immediate vicinity. The
elevation of the pass above the sea, as determined by a single reading
of the mercurial barometer, is 12,C90 feet.
We made station 17 on a table a short distance southwest of the pa8&
From this vicinity a good view of a number of the most rugged of the
quartzite i)eaks may be had. Those that appear range in height from
13,600 to 13,800 feet. After camping overnight on the head of the Bio
Grande, the next day we made station 18 on a peak between Pole and
Lost Trail Creeks, whose elevation is 13,656 feet. From this pe«dc we
had a good view of the country south of Lake Fork. In this vicinity
are scattered a number of pretty high peaks, but they are generally iso-
lated from each other, and have none of the massiveness of the mount-
ains about the head of Lake Fork and the Animas. In ruggedness
they cannot compare with many that will be described further on. To
the east the slopes begin to be more gentle, and at a distance of a few
miles appears a pretty extensive plateau surrounded by high blnffiB.
The next day, in passing down the Bio Oraude, we noticed a very peca-
liar formation consisting of a very bright-green- colored rock weathered,
into little needles and spires. It is situated against the south side of
station 18. After camping near the junction of Lost Ti^fkil Greek wit^
the Eio Grande, we made two stations on the high plateau, just to the
east of the camp. The climb was very difficult on account of the great
masses of fallen timber we encountered and the bluffs that came in our
way. Once on the top of the plateau, the riding was very easy. It was
covered with loose rock, (trachyte,; but not so much so as to serionsly
impede our course. There being no prominent point, we were compeileii
BHODA] GEOGRAPHY — aA.N JUAN MOUNTAINS. 469
to make two stations. Ko. 19 was made on the eastern part of the north
edge, No. 20 on the west. This plateaa may be said to cover aboat five
square miles ; the elevation of most of this is over 12,000 feet. The
eastern part slopes off quite gradually, while on the northwest and south
the plateau terminates in nearly vertical bluffs which in many places
are several hnndi^d feet in height. To the east of this the ground )je-
coaies more and more even, till at a distance of about fifteen miles down
the river Bristol Head rises abruptly to an elevation of 12,800 feet.
From this position it appears in profile. From station 2, a series of
high plateaus extends southward all above timber-line, and ranging in
height from about 11,500 at the lowest point, a few miles north of Bris-
tol Head, to about 13,000 feet, near station 2. Southward from the low-
est point, the plateau slowly rises till, after culminating in the bald sum-
mit of Bristol Head, it falls suddenly 4,000 feet down to the Eio Grande,
and so terminates. From station 19, a grassy slope, which we afterward
found to be Antelope Park, seemed to extend to the bluffs of Bristol
Head, but after looking with the field-glasses we saw that a caiion inter-,
vened. But look at it as much as we wonld^ there was a peculiar ap-'
pearance about it we could not then explain. From station 20 we had
a splendid view of the Eio Grande Pyramid, which was eight miles dis-
. tant, and across the river from us. This is probably the finest view that
can be had of this beautiful mountain. Its pyramidal form is almost
perfect, while at the same time there is just enough bloff intermingled
with tihe dibris slopes to give relief without the usual accompaniment of
coarseness.
We left the plateau quite early, as we had a long distance to travel
before reaching camp. The pack-train, according to orders, had traveled
np the creek which comes into the Rio Grande from the south, a little
l>elow the mouth of Pole Creek. We proceeded without delay to fol-
low them. At first the riding was quite easy. We passed several salt-
licks, which were tramped full of tracks of deer and mountain-sheep.
Soon the canon narrowed in and traveling became very difficult. - We
found no trails, tracks, or signs of any kind to indicate that anybody
had ever gone up the creek before us. At several points the traveling was
very dangerous; at one place that I now recall to mind it was espec-
ially so. The creek at that time was a considerable stream, and, from
the great fall it had, was a )>erfect torrent. The bed was filled with
large stones, and among these the water boiled and foamed terribly.
At this point we had to slide our mules down a very steep, rocky slope
of about 100 feet in height ; at the bottom there was scarcely room
enough for a man to stand conveniently between the slide and the stream.
Just above this point was one of those deep pools where the big trout
love to dwell, while at its lower end tlie water rushed through between
several large rocks like a mill-racei Now the only way to cross was jnst
at the lower end of the pool, where the water was shallow ; below, the
current was dangerously swift ; above, the water was 6 or 7 feet deep.
Lea\ing the mules and instruments with me, Wilson scrambled across
•to the other side, and I threw him his mule's rope, and while he hauled
I whipped the beast behind. After a few minutes of this treatment,
with the asinine obstinacy fbr which this particular mule was famous,
she leapt out into the pool and, swimming up to the head, tried to climb
up a smooth, wet rock, but did not succeed. After a thorough stoning
she finally returned to me, and we repeated the experiment, this time
with better success. Next, my mule, *' Bones," was taken in hand.
Having passed through the Valley of humiliation the year before, and
probably having taken mental notes on the disgraceful failure of her
470 GEOLOGICAL SURVEY OF THE TERRITORIES.
comrade's first attempt, sbe <' made the riffle" with little trouble. Other
experiences of a little less exciting nature served to heighten onr dislike
for thiH creek. Having climbed over 2,000 feet in the morning, and
made two stations, we felt very tired, and oar males walked slowly.
Alter a while darkness began to come on, and camp did not appear.
^* Bones" began to take on that pitiful look engendered by her horror of
having to stay out. Every time that such a contingency seemed prob-
able her lower lip would fall and hang down in a strangely sorrowful
way. )She seemed to recall that awful night in the Greenhorn Afouo-
tnins, in 1873, when she slept out away from her companions^ and wherp,
sifter several months of nnceasing labor, that one night broke her dowo
and made her lip hang down as it never hung betbre and never did
»gain. Soon, J;iowever, we came again upon the tracks of the traio. and
her long ears pricked up and she became so excited over it that I could
fe'Ciircely keep her in a walk. When the camp-fire appeared and she got
the scent of her companions, she seemed pertectly happy and conteoted,
u» we were also. For some distance below camp the stream-bed bad
'widened out into quite a little valley, which continued above camp up
to the head of the stream.
The next day, August 22, we made the ascent of the Kio Grande
Pyramid. The day was beautiful to its close, a remarkable circumstance
tor this season of the year iu these mountains. As we were camped at
the foot of the mountain we had plenty of time. Wishing to give the
mules a little rest, Mr. Wilson directed Ford, one of the packers, 4o fol-
low after and bring them back to camp. We rode up the west slope of
the mountain to near 13,000 J'eet elevation. Taking off our instrumeots,
we threw the stirrups over the saddles, and fixed the bridles and ropes
so that they could not get caught in the timber. We then tried to start
the mules back to camp by throwing stones at them. They would move
off a little, but if we tried to drive them farther they would dodge back.
The reason seemed to be that they had noticed that camp always was
made in a different place each day, and they were afraid of getting loat
if they strayed off. Their great horror of gating lost was very notice-
able iu many cases. In every case where we had to hunt for the camp
after dark, they seemed to give up entirely and put their whole trust in
their riders. Often have we left them loose, at elevations ranging Irom
12.000 to 13,000 feet, tar above the timber-line, but they never at-
tempted to stray away, although they would crop whatever grass they
could find near. At times when they could not be tied so as to get
enough grass, we would take oft' saddle and bridle, and leave them per-
fectly lo He, but it seemed to make no difference.
The climb on foot was quite easy, and was not more than aboat
1,000 feet vertical. On the top we found a nicel^^-built monument
of stones, which we increased in height to about 6 feet.- Some
enterprising climber seems to have taken a just pride iu leaving his
mark on this beautiful t>eak. The fact that the monument was on the
ifue snmmit indicated the fact that its builder was something else than
a common miner. The height of this ijeak (station 21) is 13,773 feet .
above the sea. The view from here is very fine. The whole mass of
the quartzite peaks, so often mentioned as prominent features in the
views from previous stations, from here stand out clearer than from
any point yet visited. Almost all of the higher points are clearly vis-
ible, but they are massed together in such a way that from this point
the drainage of the system cannot be made out at all. In one place,
to the south of us, we coul.d see low rolling country, indicating that we
were near the southern termination of the high mountains. To tbe
BuoDA.] ^ GEOGRAPHY QUABTZITE PEAKS. 471
east the view was ver^' extensive, maiiy poiuts of the Sangre <le Ciisto
range, east of San Luis Valley, being clearly visible at a distance of one
Landred and ten miles. In the desciBnt nothing of special interest trans-
pired. The next da^v camp was moved np near the timber-line, at the
bead of the creek, while the three of us followed up a branch coming
in oo the east side, and, crossing the naitioual divide, made station 2^,
on the southern point of a granite ridge, at an elevation of about
13,000 feet. The divide here is very near tl>e boundary between the
trachyte and quartzite. This line marks a sudden and decided change
in the nature of the topography. Station 22 is on granite, the first we
had yet come across in the district, but it only appears here in a small
area. Before leaving we were again visited by an electric hail and rain
storm, which soon cut short all work. Although surrounded by high
peaks, rising several hundred feet above us, the phenomena seemed
quite as marked as at any previous time. The whole mass of peaks west
of us was soon veiled inclouda. Just as we were leaving the little knob
on the end of the ridge which had formed our station, we all felt a
heavy shock as if from an electric battery. Being unaccompanied by
thunder, we concluded that we had been subjected to a miniature stroke
of lightning. This is the last station ' where we felt any. electricity,
although we were often caught on the peaks in rain and hail storms.
The next day we had a storm almost exactly similar to this one, onl^'
it was entirely unaccompanied by electricity. The date of this station
(station 22) was August 23. The rain cootiuned falling during our ride
to camp, which we found located in a clump of pines, at the junction of
two small streams. Like all the trees near the timber-line, these had
few branches, and furnished us little protection from storms.
Next morning the sky was pretty clear, so, without moving camp, we
crossed the divide south of us, and ascended the high quartzite mountain
east of the Yallecita This quartzite rock is very hard, and breaks
off in angular fragments with almost polished faces. Where d^bris-slideB
are formed of these fragments it is found that the rocks slip and
slide on each other very easily. Sometimes we would step on a stone
weighing several tons; it would tip up, as if delicately balanced, or slip
from under us. These seem to be universal characteristics of quartzite
dibris^ so that in climbing over it great care is required. This peak was
very steep and difficult to climb ; in fact, more so than any which we
had yet ascended. When we had nearly reached the summit, and at an
elevation of 13,600 feet, a small grizzly bear suddenly jumped up a few
yards in front of us and rushed down the steep slide on the south face
of the peak. Of course, in a climb as long and difficult as this, our instru-
ments and books were all we cared about bringing with us, and for this
reason our guns were leit behind. We were .much surprised to see an
animal in this place. It is ever thus ; when you feel you are treading
a path never trod by a living thing before, and your imagination begins
to build for itself a romantic picture, if some such vile, worldly thing aH
a paper collar or a whisky-bottle does not intrude itself on the sight, some
beastly quadruped needs must break the precious solitude and scatter
your airy castle to the winds. To show onr utter disgust for all animate
things that could not live below this altitude, we yelled and threw stones
after the bear till he finally was lost to slight far down the mountain-
side, lu our hate we even wished he migbt have been in a position
whence we could have rolled rocks down on him. As we passed on we
saw several places where he or others of his breed had scraped out be<ls
amoDg the finer debris. They seemed to have come up here for fresh
air, or to sun themselves, or both. Alter this experience we named the
472 QEOLOOICAL SURVET OF THE TERRITORIE&U
peak Mount Oso, from the Spanish word for bear. Aa we neared the
top of the peak the cloada coming from the west began to toacb the
sammit, and we expected that the electricity woald prevent any work.
As we came up into the cloud we felt no electricity, at which we were
much surprised. Setting up the instrument, we worked for abont ao
hour, getting sights through the clouds, for as yet the storm bad not
fully commenced. The height of this point is 13,640 feet.
A number of sharp, distinct peaks, all quartzite,rise up in this vicinity
from 2,000 to 4,000 leet above their bases, and all are very steep and rag-
ged, more like needles than mountains. A number of little lakes are dot-
ted here and there at the heads of the canons. To the we^t, across the
Vallecito, the view into the high quartzites was ranch obstracted hy
clouds. To the northwest, at a distance of about six miles, in the center
of the group, was a high peak of vertical stratii, and all the upper
portion formed of great vertical pillars of quartzite. It seemed to be
on the center of upheaval, as on the two sides of it the strata inclined
in different directions. Its elevation is about 13,783 feet.
In the immediate vicinity of our station the strata dipped at ever>'
possible angle, and appeared so complicated that only a very detailed
study could ever bring order out of the chaos.
In our descent from the peak we got pretty thoroughly drenched, and
found our mules looking disconsolate. We had left them near the see-
ond little lake northeast of Mount Oso.
Crossing the pass near this lake, we passed over to our camp on Rio
Grande waters, encountering much miry ground on the way. The rain
continued falling steadily all day and all night. The next morning the
creek near our camp was flooded, as were also our little tents. Kain
continued next morning, and as the elevation of this camp was 1I,G00
feet, and the timber thin and scattering, it was a poor place to remain
during a storm. We remained in camp all day. By standing in the rain
before the log fire we succeeded in drying ourselves nearly as fast as we
got wet. Hoping that it would clear off, we did not start early the next
morning, but seeing no prospect of a change in the weather, we ssiddled
up early in the forenoon and departed for other scenes. Our supply of
provisions was getting very short, and we could not remain longer.
All our flour hml already given out, while the diied apples, beans,
and even the bacon were beginning to draw to their close. With
all these solemn facts staring us in the face, the caravan started about
10 o'clock a. m. Our course lay up the creek and over the pass we had
crossed the day previous. We found the whole country flooded. Natu-
rally very boggy, the ground was now so full of water that it almost
floated.
The next morning the rain still continued. As the 5«upplies were get-
ting short so fast, we concluded to strike the nearest way for Howard-
ville. Moreover, we were getting disgusted with this part or' the conn-
try, and wanted to find a better camping-ground. A«cordiugly, we
moved up the main branch of the Vallecito. it was running considera-
ble risk, as without a trail to guide us we felt doubtful about being able
to cross the divide. The rain fell fast, and we were soon soaked to the
skin. The grade being very steep, we rose in elevation very fast, and soon
found snow and raiu falling together, and we nearly froze. We stoppe«l at
one place and made a Are by which to warm our feet, but the wood was so
soaked with water that we found it a diflicult task. The train was behind
and did not catch up ; so Wilson and I heaped all the logs that were lying
handy upon the fire, and, as we found later, the rest of the party made
good use of the fire. Near the head of the creek the sloi>e became very
steep and rose up to the divide, which, at the point at which we
BHODA.] GEOGRAPHY — QUAKTZITE PEAKS, 473
crossed it, was nearly 13,000 feet in elevation. A keen, strong breeze
did not serve to add to our comfort in our present saturated condition.
While waiting here for the train, Mr. Wilson made station 24 on a
point east of that where we crossed the ridge. The elevation of this
place is about 12,700 feet— ^a little higher than the point where we
crossed the same divide a few days ago. We traveled down that branch
of the Rio Grande which heads between stations 24 and 25, and camped
iu a splendid grove of pines. In the afternoon the sky had begun to
lighten up. Isolated clouds passed swiftly over ns from the west, ever
and anon cutting off the sunlight, and producing the sudden chilling
eflFect always noticeable in the shadow of a cloud at high altitudes. The
great difference of temperature in the sun and iu the shade at these alti-
tudes is very remarkable. At this particular time I thought I noticed
that whirls and gnsts of wind always accompanied the fast-moving
shadow. Whenever a long space between clouds allowed the sun to
shine unobstructed, for some time the air would be quite still, but the
next cloud-shadow seemed to bring with it little whirlwinds and chang-
ing gusts of chilly air. By the time we had unsaddled our animals the
sun was shining brightly, and now, after four days and three nights of
incessant rain, we had a good opportunity to dry our clothes and blan-
kets, and every one made good use of the short time before sunset. In
the evening, instead of sitting down to a hearty meal, we had to make
oar supper on bacon and dried apples nlone, and very short rations at
that. We had a few beans left, but all the bacon aud'apples were used
up for supper ; but as we expected to reach Howardville the next day,
we did not mind it very much. Our bill of fare next morning pre-
sented only two articles — beans, which on account of our elevation could
not be well cooked, and sugar. We could take either or both as we chose.
Beans with other food are very strengthening, but alone we could
scarcely eat them at all. The pack-train started direct to Howardville,
while Wilson and I climbed the most northern of the quart zite peaks, a
point having an elevation of 13,576 feet above the sea. The day was
clear, still, and beautiful. ' After riding as far as we could, we still had
about a thousand feet to climb on foot over the steep dSbris slides before
reaching the top. We soon discovered that our breakfast of beans and
sugar termed a poor foundation for such hard work. Once on top, a
row of ten distinct peaks stretched in a nearly east and west line before
our eyes. Their ruggedness may be understood from the illustration of
** the Quartzite Peaks from station 38," the three or four on the left of
the picture being just in front of us from station 25. Being much nearer,
they appeared much more rugged than from station 38. The peaks in
this row range from 13,560 to 13,831 feet in elevation. Between them
we could see the higher peaks to the south.
The great and essential differences in the topography resulting from
the change in the geological formation is here so very marked and is so
interesting that I cannot pass it by without notice. The general differ-
ence in the appearance of the country in trachyte and quartzite forma-
tions is intended to be shown by the two large topographical sketches
presented in this report. The view of Mount Sneft'els from station 20
shows nothing but trachyte rock, while the sketch from station 38 shows
quartzite only. But a mere sketch cannot show well the characteristics
of the two. I have tried to work out some of the features peculiar to
the topography of each of these two formations. These being derived
almost wholly from observations in Southern Colorado and for the great
part in 'this particular region, they may not have a very general appli-
cation.
474 GEOLOGICAL SURVEY OF THE TERRITORIES.
First, then, in trachyte or volcanic rocks, the lava>flows being for the
roost part horizontal, the rock fractures vertically, and tbe falling away
of pieces produces bluffs which are generally very nearly vertical. Mcm^-
over, from the nature of the How, horizontal lines or bands are left rnii-
uiug across the faces of all the bluffs. This latter is very characteristic
of the formation.
Second. At the bases of the bluffs dSbris slopes commence, and sweep
down generally in graceful curves to a greater or less distance.
Third. These slopes are seldom very steep for any great distance, the
great fall from the uiountaiu-summits to the valleys being by way of
high bluffs and comparatively gentle dSbris slopes. In other words, the
total fall is very irregularly distributed over tbe distance from the top
to the base of the mountain.
Fourth. The junction-line of the bluffs and ddbris slopes is almost
always distinctly marked.
On the other hand, in quartzite formations —
First. Bluffs vertical, or nearly so, are very common } except in very
raie cases there are no marked horizontal lines.
Second. The junction between the bluffi) and ddbris slopes is never
so distinctly marked as in trachyte.
Third. On account of the fact that this rock breaks off in large angu-
lar fragments, and also on account of its great hardness, it will lie at a
much steeper slope than tbe other rock. From the same causes the loose
rock does not 'take on those beautiful sweeping curves so common in
volcanic rocks, but have a certain stiffness of line.
Fourth. The solid rock, from its great hardness and the manner of its
crystallization, is often found in very steep, yet quite irregular slopes,
without taking on tbe form of bluff. A noticeable instance of this is
the most easterly of the ten peaks mentioned above. The fall from its
summit to Vallecito Creek on the east is 3,000 feet in less than a mile
horizontal, or a mean slope of nearly 32^ ; yet it is a plain slope of solid
rock, more or less irregular, of course, but having no bluff in all that
distance. On the north side of the same *peak there is a slope at
an angle of 60^ to 80^ for not less than 2,000 feet, yet there is uo
part of it bluff.
Still another point is the fact that in the metamorphism of the origi-
nal sedimentary rocks into quartzite, the great natural convulsions at-
tending that process have distorted the strsita terribly, so that, as in
this particular region, a number of peaks in a small area may each have
its strata dipping at a different angle from all the rest. The effect of
this on topography may be seen in the sketch from station 38. Tbe
high peak next to the last one on the left shows in a marked manner
that tbe strata incline to tbe right, or southward. The high peak near
the middle of the sketch, being in the center of upheaval, has vertical
strata, while those farther to the right incline to tbe north. This lat-
ter fact is not so well shown in this sketch, but from some other points
of view itapi^ears very plainly. These facts show how the form of the
peaks may differ in the same kind of rocks ; but as there is little or none
of tbis upsetting of the lava-ilows, there must result a distinct type of
mountain-form for each. The peculiar crystallization of the quartzite has
also a marked effect on the forms.
In accordance with these facts, we find that quartzite mountains are
generally much more rugged, but lacking the relief given to those in
volcanic regions by the contrast of the blnffs with the ^^6m-sIope&
The boundary of tbe quartzite on the north follows closely the national
divide.
BHODA.) GEOGRAPHY — ^HBAD OP UNCOMPAHGRE RIVER. 475
On onr retarn to Howardville we rode across the rolling ground which
extends southward from Ganningham Pass. Arriving at the town, we
found Mr. Jackson, the photographer of the expedition, with his partj.
He had just arrived from the Los Pinos agency. We made the ascent
of Sultan Mountain with him, and he succeeded in getting a number of
good photographs of the surrounding country. From this point is ob-
tained by far the best view of Bakei^s Park that is obtainable from any
peak in the vicinity.
After getting our supplies we marched up Mineral Creek, while Mr.
Jackson struck south over the trail which passed around the west side
of Sultan Mountain, and made a very interesting investigation of the
old ruins in Southwestern Colorado.
In the afternoon rain fell, and continued into the night, but the next
morning was cold and the sky clear and beautiful. This date (Septem-
ber 3) is remarkable as being the time of the abrupt change between
summer and fall. After this, till the snow-storms commenced, the
weather was cold and clear. Having camped overnight at the
junction of Bear and Mineral Creeks, the next morning we moved
up the latter, and made stations 27 and 28 on a high ridge between
Mineral and Cement Creeks. Camping near the head of the creek,
the following day we crossed the pass at its head and passed over
to the head of the XJncompahgre Biver. The elevation of this
pass is 11,100 feet above the sea. It is entirely covered with timber.
The slope to the south is quite gradual, but to the north, down the
Uncompahgre, the fall is dOO feet in two miles. Then for several miles
the stream flows comparatively smoothly, tiU it finally enters a deep
box canon, where the fall is very great. Traveling for some distance is
both difficult and dangerous. At the bottom of the first steep slope a
great area of fallen timber commences. The logs so cover the ground
that traveling is very nearly impossible. Leaving a notice for the pack-
train to camp near the beginning of this dead timber, Mr. Wilson, Dr.
Endlich, and I rode on, and finally got through the timber, when we
had open grassy ground to travel over, but the slope was so steep that
we could ride only a small part of the way. Leaving onr mules loose,
as usual, to find what grass they might at this elevation, which
was a little less than 13,0(M) feet, we made station 29, on a round-topped
];)eak, which, being surrounded by peaks higher than itself, is of no great
importance. It was taken as a station, because its position between two
of the main branches of the Uncompahgre made it a key-point for the
drainage system which forms the head of that stream. Its elevation
is 13,20G feet. From this point we got by far the best view of Mount Snef-
fels, and the curious pinnacle-forms in its vicinity, which have already
been mentioned as seen from station 10. The accompanying illustration,
taken from a hasty topographical sketch, will give a faint idea of the
great peak and its vicinity. Of course the elevation and ruggedness of
the mountains shown in the sketch can only be appreciateU by a per-
son who has climbed many mountains. Even then the air is so clear at
these high altitudes that one is deceived in spite of himself with regard
to distances. From here we could see no feasible route by which to
climb the great Mount Sneffels, so we laid the question aside till a view
from some peak farther to the west should solve it satisfactorily. Next
day we xetraced our steps over the pass and down Mineral Creek, camp-
ing again at its junction with Bear Creek. Moving up the latter stream,
we camped on a considerable branch which comes in from the north.
This is probably the finest camping-ground on the whole stream, with
fine timber, good water, and a suificieut quantity of grass. Above this
476 GEOLOGICAL SURVEY OF THE TERRITORIES.
there is a dense grove of timber, through which you pass ap a pretty
steep slope ; in a short distance the pines end, and you come out into
an open space, extending several miles up the stream, and cov-
ered with a remarkably rich growth of weeds and shrubs. This
circumstance is probably explained by the fact that here a great
part of the lower slopes of the caiion is composed of red sandstone,
which seems to produce a much better soil than the volcanic rock.
The next day (September 6) we made the ascent of the highest peak
in this vicinity. It is marked statibn 30 on the map, and has an eleva-
tion of 13,897 feet. The climb was difficult, on account of the long
slopes of loose dSbris up which we had to climb. The top of the peak
was remarkable for its smallness. It is formed of two knobs, about 20
feet apart, the northern one being a little the higher, and connected with
the other by a very sharp ridge. To the west was a slope of 60^ or liP
for 30 to 40 feet, then a precipice of about a thousand feet nearly, if not
quite, vertical. When the tripod was set up, we could not pass around
it, but had to crawl under it. We three monopolized all the sitting
and standing room on the peak. Mr. Wilson with the instrument
completely covered the true summit. Dr. Endlich took his geologi-
cal notes from the lower knob, while I sketched, sitting at the
edge of anxi almost under the instrument. The slopes, on all sides
but the narrow path we had followed, were very steep, and in a
few feet terminated in great precipices. From here we got a
splendid view of Mount Wilson, which we had seen from many
stations before this, but always across the group of mountains of whicii
station 30 formed a part. Now it rose up grandly, forming the most
massive of any peaks in our district, and, judging from its appearance
and rough estimates from the angles of elevation, we felt that it must
be very high. In line with the peak, but' several miles nearer, appeared
Lizard's Head, a peculiar pinnacle, which from this view appears quite
broad. It will be more particularly noticed farther on.
After finishing our observations, we built a small monument of
loose stones, which, when finished, covered the top so completely, that
a person could not pass around it. We descended more easily than we
had ascended, and found camp at the lower end of a long patch of
timber, near the junction of the main stream with the last tributary
which comes in from the south as you travel up. This marks the upper
end of the open, weedy area already mentioned. The total climb from
our last night's camp to the station was 4,000 feet, and the descent to
our present camp 3,200 feet. On the day following we let camp remain
where it was, and rode up the creek to the south of us, and over the
divide, to Engineer Mountain. On the way we had to pass around a
peculiar amphitheater, which had been eroded out of the red sandstone.
The stratification of the sandstone had produced benches, which extended
all the way around the head of a little stream which flows into Caecade
Creek. VVe found the ascent of the peak not very tiresome, but rather
dangerous. We climbed up the ridge from the east. On our right was
the great bluff*, which is nearly a thousand feet in height and almost
vertical. On the southeast side the rock weathered off in small plate-
like fragments, producing innumerable cracks and little shelves, bat
none large enough to give a secure foot-hold. The slope on this side
is very steep, so that if a person should slip he could not possibly
save himself from destruction. Mr. Prout in 1873 ascended this same
peak from the south side, which I should judge is much the safer, but at
the same time the longer and more tiresome way. From this point we
had a splendid view down the Animas.- Animas Park was visible, and
RHODA] aEOGBAPHY — HEAD OP SAN MIGUEL BIVEfi. 477
the low country in its vicinity showed us that the high mountaius were
nearly at an end. A group of pretty high peaks were to be seen to the
southwest/called the La Plata Mountains. They are completely isolated
from the main mass of the range by many miles of comparatively low
land.
On our return to camp a sudden and heavy shower of rain came up,
but cleared off soon after. The nest day found us on our way through
the patch of timber already mentioned. The trail passes through t^e
center of the group, which is very swampy, and our animals mired
many times before we got through. We found relief only at the timber-
line, after which we rode on, over grass and fine rock-slopes, up to tho
pass, which has an elevation, according to our aneroid barometers, of
12,600 feet. It is certainly the highest of all the passes leading out of
Baker's Park. A pass which I think will be found much better, crosses
the range about six miles to the northeast of this. To go this way you
must travel up the largest tributary of Mineral Greek, which comes in
from the west, and cross over on to a tributary of the Ban Miguel. This
pass is not less than a thousand feet lower, and, at lea^t to the west,
has a much better grade. Passing over from Bear Creek to the head of
the San Miguel, after a sudden descent of several hundred feet, we came
to a small lake. Further dowo, the slope was more gradual for some
distance, till we came to a steep debm-slide, down which the'trailled to
the valley below. The fall from the pass to the valley, by way of the
trail, is 2,800 feet in two miles. On the east side of the pass the rise
from the stream-junction, where we camped, to the pass is 2,000 feet in
two miles.
Station 30 rose up boldly just to the north of us as we rode down the
trail. Its side was worn out into beautiful forms, and the delicate
blending of the dull red and yellow colors of the rocks, taken together
with the long sweeps of the d^6m-slides, gave this peak a finer ap-
pearance than any we had yet seen. Once down in the little valley be-
low, we found trees and grass growing very luxuriantly.
1 he trail crosses several boggy places, over which our mules passed
with difficulty. A few miles down stream from the head of the little
valley is San Miguel Lake, a very beautiful sheet of water, filled with
fine trout. We stopped to make a compass station on the edge of the
lake, and took a reading with the mercurial barometer, which makes
the elevation 9,720 feet. Thence we traveled down the San Miguel
liiver, along a very old, disused Indian trail; in some places, con-
siderable trees lying across it showed that it had not been used for
many years. For some distance below the lake, the San Miguel, which
is here a pretty large creek, flows quite gently; but further dowii
the slope suddenly increases, and the stream is broken up into falls
and cascades. In going down the trail, at this point, we found
tLe slope so steep that we had to dismount and lead our mules, till
we reached the bed of a large creek which comes Into the San Miguel
from the east. After crossing this the trail ascends the north slope
of the canon, which is quite steep. The total fall, from the lake
down to the junction of this creek with the main stream, is about 900
or 1,000 feet in a distance of two and a half miles. At least GOO feet
of this fall takes place in the last mile. At the bottom is a fine full, which
from a distance we judged to be not less than a hundred feet in height.
After crossing the canon of the creek above mentioned we came out on
a pretty smooth area, covered with scattering timber and fine grass.
One thing very peculiar about this particular part of the country is the
deathlike stillness that almost oppresses one in passing through it.
478 GEOLOGICAL SURVEY OP THE TERBITOKIES.
There is tbe fiuest growth of grass I have ever seen in Colorado, with
beautifal little groves of pine and quaking asp scattered about, whieh
one would expect to be full of game. The old trail and the very anti-
qaated appearance of the carvings on the trees, and the absence of all
tracks, old or new, indicated that the Indians had abandoned this roote
long since. With all these conditions, so favorable to animal life, ve
did not hear a bird twitter in tbe thickets, and saw neither deer, elk, nor
antelope, nor even a single track of one of those animals. In all other
parts of the country little squirrels and chipmunks were seen in abun-
dance ', but here, if they existed at all, they kept themselves close. We
made camp on the large east fork of the San Miguel, just across the
stream from station 32 on the maj). The next day, September 9, we
made station 32, on a low hill on the north side of tbe creek, which from
its width might more i)roperly be called a river. Above this for several
miles the stream bed is very flat and covered with willows, while tbe
stream itself winds like a great snake. A short distance below our sta-
tion the stream plunges down very abruptly into the caiion of the San
Miguel, which, above and below this junction, cuts down from 800 to
1,000 feet into the sandstone which here makes its appearance.
Leaving station 32 on our way to Mount Sneffels, we followed tbe
trail a short distance, and then, turning off to the right, with great diffi-
culty succeeded in descending to the bed of a creek flowing fn>m the
northeast. In this vicinity we saw a band of six gray wolves, the fin^t
we had seen during the season.
With great diflBculty we followed up the cafion, which gradually be-
came narrower and more rocky. In some places we had to cross over
short Spaces of smooth, almost polished rock-surfaces, inclined toward
the stream. In one such place a small rivulet of water flowed over the
surface and terminated below in a fall of considerable height. Tbe
smooth stone, thus wet, rendered our passage with the mule-train very
hazaidous, as the least slip would have resulted in the certain destruc-
tion of an animal, and possibly serious injury to members of the party.
As we traveled upward the trees became more and more scattering,
and the huge rock-slides, which below we had only seen high up against
the mountain-sides, began to extend their Angers, like glaciers, tar below
the timber-line, and in many places reached the bed of the creek. These
slides, ever and anon crossing our path, rendered travel very difficult
for animals ; the more so as they were composed of large angular frag-
ments, often many tons in weight, and containing in their interstices no
vestige of soil or vegetation. Sometimes wo were able, by filling in the
spaces with small stones, to form a I'ough trail over these. At others,
we were able to go around them.
The obstacles to our onward march continued to grow greater and
greater till we came to the upper verge of a clump of trees, and found
our further progress completely barred by the great (2^^m-slides on
both sides of the creek, coming down to the water's edge, making tbe
passage for animals an utter impossibility. About half a mile farther
on we could see the trees commence again; but this strait, if we may
call it such, was too much for us. Besides, we could see no prospect of
good grass for the animals ahead, while this laat group of trees foroied
a beautiful camping ground, and was overgrown with a rich crop of
grass. There, then, we made camp ; and as it was early in the afternoon,
and the sun shining brightly, we took this rare opportunity of spreading
out our blankets to dry. Wilson turned out his mule with the rest to
i'eed, and walked on over the rock-slides, up the canon, to reconnciter,
and after a long and tiresome walk reached the summit of the pass at
BHODA.] GEOGRAPHY — ^ASCENT OP MOUNT SNEPFELfi. 479
the bead of the gnlch, and saw, far across, a carioas sink-like amphithea-
ter, the object ot onr jonrney, looming ap in terrible blackness before
bini. He saw at a glance that from oor present positioD the peak mast
be ascended in one day, from our present camp, all on foot, The mount-
ain had to be climbed, and the only easier ascent was from the north.
Bat to get to that side of the mountain necessitated a circnitous journey
of several days around the portion of the mountains jutting out to the
west.
On his return to camp in the evening he reported the result of his
deliberations to the rest of the party, and it was concluded to make the
ascent from our present camp. We all knew well that the winter-storms
would soon commence, and we could ill aftbrd to lose the time necessary
to go around to the north side of the mountain. The present camp is
marked on the map as camp 45.
ASCENT OF MOUNT SNBPFELS.
The next morning we provided ourselves with lunches, as was
our custom, and the three of us set out on foot at six o'clock, with
onr note-books and instruments. The first portion of the climb
to the pass above mentioned, was in a northeasterly direction from
camp. After crossing the portion of debris already described we
came again to timber, then to soil covered with very short grass
but devoid of other vegetation. After leaving the timber we could see
about us, and a dreary sight we saw. !Near us was nothing but these
great angular fragments of tra-chytic rock, which, in the distance, faded
to a dull, dreary, gray tint. In some places these slides formed long,
regular, slightly curved lines; in others the stone appeared in swells
like sand-dunes. The head of the cation was amphitheatrical in form,
like almost all in lava regions. On the east side we noticed particularly
a sub-amphitheater, which, being composed of nothing but the loose
d6bri8, variegated by neither shrub nor blade of grass nor even barren
soil, nor by any change of color in the rock, presented one of the most
desolate sights that meets the eye of the mountain climber. The weird
stillness of high altitudes, only served to heighten the appearance of
desolation about us, and gave one the idea that all nature was dead.
Passing from the small area of soil over which we traveled after leav-
ing the timber, we came again to the loose debris. Take note of that
little patch of soil, for we may not step on soil again till we return at
night from our tiresome climb. We now had to walk over the loose
bowlders, stepping Irom stone to stone. This was very tiresome, as we
could not relax our attention for a single moment for fear we should step
OQ a balanced stone, and fall or slip on some smooth suifaee. Toward
the last, the asceut became very steep, and we had to climb with great
care. The last few hundred feet was just about as steep as loose rock
would lie. We thought nothing of this, however, as we were fresh, and
knew, besides, that this was the easiest part of our day's journey. We
reached the pass at last, and as we had been climbing till then in the
shadow we were glad to see the sun rising clear and beautiful. Every-
thing seemed to conspire to make a beautiful day, and we 'lacked ouiy
time to let our imaginations run on and make a sublimely-romantic pic-
ture of sunrise at a high elevation. The claw-marks on the rocks, on
either side of the summit of the pass, showed that the grizzly had been
before us. We gave up all hope of ever beating the bear climbing
mountains. Several times before, when, after terribly difQcult and
dangerous climbs, we had secretly chuckled over our having outwitted
480 GEOLOGICAL SURVEY OF THE TERRITORIES.
Bruin at last, some of the tribe had saddenly jamped np not far from
us and takea to their heels over the loose rocks. Mountain sheep we
had beaten in fair competition, but the bear was '^ one too many for ns.*^
After stopping a few moments to draw our breath, we had a little
leisure to look around us. Looking back we could see the clump of trees,
3,000 feet below us, in which camp was situated ; wbile in front of us, and
behind us, and around us, appeared nothing but miles and miles of loose
rock, with rocky peaks everywhere. Immediately in front of us was a
curious depression, which, at its lowest point, was about 2,000 feet below
us, although we were standing on the lowest point of the ridge surround-
ing it. It covered several square miles in area; it seemed to be com-
pletely closed up, as no outlet could be seen. It was apparently walled in
on all sides. On our right a bluff ran clear around to the great mountain,
and was very nearly vertical for full a thousand feet, at some points more.
For three miles from this pass, along the ridge on the south side of the
amphitheater, no point is less than 13,500 feet in elevation, while several
peaks rise above 13,700, and one above 13,800 feet. Just to the Bouth of
Mount Sneffels was another comparatively low gap, which we felt was
passable for good foot-climbers. This and the pass on which we stood
were the only visible outlets; excepting these two, which were only jusc
passable to men on foot, we could see no break in the great Chinese wall
around this little empire of desolation and deathlike stillness. We knew,
of course, that there must be an outlet, and we knew where that outlet
must be, but we saw none ; we knew that the wall around the south
side from us to the great i)eak, was continuous, and we could see that
there was no break in the north wall for a considerable distance. The
only point we were not sure of was at the northeast corner of the basin,
just west of the peak. We were certain the outlet must be there, merely
because we knew it could be nowhere else; however interesting it might
have been from a geological point of view, it made our hearts sink within
us to look at it. In making the ascent of a mountain, there is nothing
more painful than to find a deep gorge or sink crossing your path; you
know that all the distance you go down must be climbed up again before
you reach once more your present level. We did not remain on the pass
long enough to think half that I have written, for it has always been a
maxim with us that every minute saved in the 'morning brings us back
to camp so much earlier in the evening, and we can never tell how long
a climb is going to take us. We find sufficient time while climbing to
observe the scenery around us in a very general way, but the romauoe
of our work is not fully appreciated by us till we reach civilization, where
we can find leisure to think over what we have seen ; at the time no
romance is visible.
Almost due east of us and across the sink, at a distance of three miles,
was Mount Snefi'els, the end and aim of our labors. We traveled over
the sunken area a considerable time, as it is several miles across. As
we went on, it became more and more evident that the '' fallen in " ap-
pearance of this depressed area was not mere appearance. Evidence
pi*esented itself on all sides to prove that this great area had actnallf
sunk in one mass several hundred feet. After a time the descent b^ame
much steeper, and we were much surprised on looking back to see be-
hind us a peak rising up to a considerable height. The truth was, that
it was only a ridge the same height as the main part of the amphitheater,
and only presented the appearance of a peak from below. Near this
point we were joined by Ford, one of the packers, who had concluded
that he wanted to climb a peak, too, and had chosen this oue^ the hardest
climb of the season. The lowest point of the amphitheateir was the head
BHODA.1 GEOGRAPHY — AMOUNT SNEFFELS. 481
of a cnnon leading oat to the north. In the bottom of this was a small
lake with an elevation of nearly 12,000 feet. It was rather a pleasure
than otherwise when we began to ascend again. Now we were sure that
"we had no more gorges or sinks to cross, bat that, excepting the aps and
downs common to all peaks, our way lay upward. A few hundred
feet above the bottom of the sink we came upon a bench on which
were two small lakes, while just beyond, the steep, rugged monutfiin
rose up. The first half of the height was very steep, but neither so tire-
some nor so dangerous as the last half. The first was a plain slope ex-
tending from the Jakes to the ridge of which the peak formed the termi-
nation. After reachin&r this we had to follow the sharp ridge of the
mountain, which for a considerable distance was notched much like a
comb. The crystallization was nearly vertical, and we could not follow
along the highest line of the ridge, but had to go down the spaces be-
tween the teeth of the comb, then climb hand over hand up the steep
bluff beyond, and soonuntil, within a few hundred feet of the top, the rock
suddenly changed and was worn into more or less rounded slopes, all con-
siderably polished, but beveled out in a curious manner, by the weather.
These slight bevels were our only foot-holds, and, as the slope was quite
steep in some places, we had to climb with care ; but all our labor
was soon rewarded by the glorious view which pre8ente<l itself to us
when we reached the top. On the west and north sides the peak was
precipitous, while on the east it sloped much more gradually. It was
situated on the extreme north edge of the range, and fell in very steep
slopes to the low valley of the Uncompahgre, to the north. On all
sides but this we were surrounded by rugged peaks and impassable
canons. The great fact which was instantly impressed upon our minds
was the great area of the surface above timber-line. In fact, toward
the east, south, and west, with the exception of a clump here and there^
at great intervals, no timber was visible. Leading from the southeast
side of the peak was a canon, which, for a considerable distance down,
ran nearly due east, but continually veering more and more toward the
north. For several miles down, the slopes to the bed were very gentle,
and presented the appearance of a deep hollow rather than that of a
gorge; but it became more and more rugged toward its mouth, till
finally, within a few miles of that point, it was almost impassable, till
at last it joined the truly great canon of the Uncompahgre River. This
latter canon and its vicinity is one of the most curious places in the
district. The ridges running down to it both from the east and west
sides are curiously notched and cut into strange shapes. Numerous high,
sharp pinnacles, clustering together here and there, appear like church-
steeples, while in other places the weathering of bluffs has produced
the appearance of niches with statuary. We noticed several large
quartz veins which seemed never to have been discovered by the miners.
Across this space, and far above it, we saw Uncompahgre Peak, which
showed us the familiar precipice on the north side, with the terraced
slope on the south. Though presenting to our eyes the same profile as
when we were approaching it from the east, we had lost much of our
awe of the mountain from the fact that we had found so many that wore
harder to climb. We could see distinctly every station we had been on,
so far, this summer, besides many of the year previous. The group of
quartzite peaks stood up as boldly as ever about thirty miles to the south-
east. In fact, I may state here that we have never yet seen the group
from any station (and we have viewed it from all sides) without feeling
both deep respect and awe for their terrible ruggedness. The fact al-
ready stated, that the storm-clouds seem to hover about them before
31 H
482 GEOLOGICAL SURVEY OF THE TERRITORIES.
Starting on their meandering ways, only served to add to onr otber feel-
ings one of uneasiness. It may be that the vivid recollection of a loof
and dreary storm encountered in that region, made it appear to as is
an exaggerated form. A little nearer, and slightly to the left of them,
we could plainly, see and distinguish all the peaks surrounding Baker^
Park and the great mining region. Still nearer, and seeming almost
under us, was station 28, with its associates, in the little cluster of deep
red-colored peaks along the waler shed, between Mineral Creek and the
Uucompabgre. The view directly south of us presented the greatest
mass of peaks to be seen in any direction. In that direction we look
longitudinally along the range of |)eaks which forms the west line of the
great mountain-mass, from which there is a very abrupt descent to the
western plateau system. Chief among these stood station 30, which we
had visited only a few days before, while about nine miles to the we^
of it was the high peak which we were soon to climb, but whose top
was veiled in clouds, only the massive base and a few of the subordi-
nate peaks being visible. West of it were several low, sharp peaks
scattered here and there, but these soon sloped off into the plain, which
extended to the horizon, broken only by the deep canons which have
been cut in the red sandstone by the streams. Directly to the west, in
the far distance, was the group of the Sierra La Sal Mountains, and
scattered about the horizon, south of them, we could see several very
distant mountains, which were so far away that their blue color conld
scarcely be distinguished from that of the sky. Immediately to the
north of us, and far below us, was the valley of the Uncompahgre, which,
on both sides, seemed to have quite a gradual slope toward the stream.
To us, viewing it from this great elevation, it presented the appearance
of being covered with a rich growth of grass, though of this fact we
could not be sure from so great a distance. The junction of the Uuoom-
pahgre with the Gunnison was distinctly marked by the vegetation along
the banks of the two streams. We could see the course some distance
below the junction, but it soon faded into the distance, and no one coold
say, from what he saw, what way the water had gone.
Beyond the Gunnison, on the north, there appeared a very elevated
plateau, which, commencing near the mountain-peaks, presented a nearly
horizontal protile for a considerable distance, and then, slowly increasing,
its slope fell off almost insensibly to the west. Still farther around to
the right, and about northeast of us, we could see most of the great peaks
west of the Arkansas Iliver. Many others appeared behind, but we did
not trouble our minds about recognizing them, sis all our time was neces-
sary for the more immediate details of the to|>ography around us. The
great length of time requited to ascend and descend again prevented us
Irom remaining long. We had reached the top about noon, and found
that we could not possibly remain over two hours and exi>ect to get to
camp ; and since there was not a stick of timber on the way we dared
not sleep out, even though the work on the peak had to be cut short
Our time being up, we raised a monument of loose stones about five feet
high and started for camp.
The descent to the lakes was very easy and did not require much time,
but, as we expected, the climb up to the pass again began to tell on us,
and a weakness in our legs showed what a terrible strain on our systems
the morning's climb had been. We finally reached the pass just in time
to see the sun setting. Some may suppose that now we sat down and
rested ourselves before making the last descent down to camp. But all
frequenters of the high mountains are acquainted with the fact that
there, darkness follows sunset very suddenly, with scarcely any twilight
between. By calling to mind this iact and estimating the obstacles
vBOj>A,} GEOGRAPHY — ^MOUNTAIN CLIMBING. 483
between us and camp, we found' that with our ntmost endeavors we
coald not hope to get into camp till long after dark. On the other hand,
we knew that we could not travel any considerable distance over the
debris after dark, so we struck for the timber with all our speed. When
darkness came on we found ourselves in a mixture of vi^getation and
]oose rock, and had to pick our way with the utmost care. Our long-
ooiitinued exertions were at last crowned with success, and we had
the pleasure of sitting down to a supper which tasted to us far better
than the most costly meals of civilization, served up in the most expen-
sive hotels. We reached camp at eight o'clock in the evening, having
been fourteen hours from camp, twelve of which had been occupied in
steady climbing, and two in work on the summit of the peak. During
those twelve hours we had climbed up 7,000 feet, and down an equal dis-
tance, beside traveling a horizontiil distance of six miles, the whole over
loose rock.
The next day, which was September 11, we retraced our steps down
the creek, and turning to the right followed up the west branch of the
same stream. We made station 34, whose elevation is 12,997 feet, on a
peak at the head of this creek. It is the most western of the great group
of mountains of which Mouut Sneftels is the highest point. From here
Lizard's Ilead, ea«t of Mount Wilson, stood up like a high monument on
the top of a mount-ain-peak. From this view the width of the base bears
about the same relation to the height as in the great artificial monu-
ments. The height of the column is 290 feet, and the elevation of the
summit above the sea 13,160 feet. From this point it is fourteen miles
distant in a straight line, yet it loomed up finely. On our way to camp,
which we found located at the junction of the two creeks, we saw a black
bear, the fii^t we had yet come across, but he disappeared so suddenly
that it was impossible to get a shot.
We were well satisfied with having finished this part of the mountain
country. Only one peak of which we had any dread remained yet
to be ascended, and that was Mount Wilson. From various circum-
stances we had reason to believe that this was higher than any sti.tion
we had yet made, and from its nigged ap))earance we dreaded its
ascent not a little. We returned to Lake San Miguel by the same trail
we had come. On our way we saw a few cranes, which, with their long
legs and unearthly noises, only served to add to the funereal aspect
of the scenery. At the lake Dr. Endlich and I stopped to make a de-
tailed sketch of station 30. From here the peak, with the lake in the
foreground, and the rich groups of pine and aspen, separated by spaces
covered with a rank growth of grass for a middle distance, presented a
beautiful appearance. Crossing over the divide between the San Mig-
uel and Dolores, at an elevation of about 10,200 feet, we turne<l off to
the right and cam|>ed on a stream which fiowH down from the southeast
side ot Mount Wilson. On the way Mr. Wilson succeeded in killing a
fair-sized male grizzly with his Springfield needle-gun.
September 13 was devoted to climbing the great mountain. Biding
to the timber-line, we sent our mules back to camp by one of the pack-
ers, and commenced the ascent. At first we had a low blnff of slate to
get over. The x>lates of the stone were remarkable for their great size
aud freedom from cracks. Above this the climb was quite easy for a
considerable distance, being nothing more th;iu plain slo|)es of loose
dibris. When we had reached an elevation of about 13,W0 feet, we
noticed three mountain-sheep on the top of a high ridge to the north of
us, and about 1,000 feet above us. We could scarcely see how they got
up there, such was the ruggedness of the ridge. They watched our
484 GEOLOGICAL 8URVEY OF THE TERRITORIES.
progress from this elevated stand-point with great interest, now and
then jumping upon a rock to get a better view. They reminded m
very much of some of the illastrations in the school geographies. A
little farther on we came to a large steep snow-bank, np which we
climbed with difficulty, cutting notches in the snow for footholds. At
the upper end of this we came to what was much worse, very steep
and dangerous rock-walls. From this point to the summit tho stone
is crystallized into vertical blocks, broken up so as to be very insecure.
Near the beginning of this part we came to a notch in the narrow
ridge which was tilled in by a great stone, with its upper part wedge-
shaped. On the east was a fall, very nearly vertical,^ of two or
three hundred feet, terminating below in the steep snow-bank already
mentioned. On the west was a precipice many hundreds of feet ia
height. Over this wedge we had to pass by straddling it and sliding
ourselves carefully across. The whole distance was not more than ten
or fifteen feet. It seemed very much like crawling along the comb of
the roof of a very high house. Just beyond arose a steep rock-wall of
loose shelving rock, np which we climbed with great difficulty, from the
fact that all the rocks were loose; and even the largest coald not be
surely depended on. Beaching the summit of this we had to walk for
forty or fifty yards along the sharp ridge over loose blocks of stone
standing on their ends. The ridge was so sharp that we had to follow
the center. On either side the slopes were so nearly vertical that If a
person should once slip there would be nothing to stop his descent for
many hundred feet, and in some places a thousand feet or more. All
the stones were so loose that we could feel them move under our feet.
For a part of the distance we had to walk straight, without anything to
lay our hands on. At one point in particular, we had to leap across a
break in the ridge where a stone had fallen out, trusting to Providence
for the firmness of tho new foot-hold. This was at an elevation of
nearly 14,200 feet. We came very near giving up here; but we could
just get a glimpse of the main peak a little farther on, aiid the tempta-
tion was too strong for us. After getting over this very dangerous part,
we came to a deep crevasse which cut across the ridge, and succeeded,
with great difficulty, in getting down to the bottom of in. A thin
coating of ice over many of the stones, remaining from a recent hail-
storm, added greatly to the danger of the climb. Thence we had to
climb aronud the edge of a bluff, which we found a very dangerous un-
dertaking. Once over this we climbed out of the crevasse without
difficulty and gained the longed-for summit. We found it composed
ot the same rock as I have described, crystallized in vertical prisms,
but crumbling away. Beyond a space probably eight or ten feet square,
we could not pass without the very greatest danger of being precipitated
over the terrible blnffs surrounding us on nearly all sides. We coald
scarcely find space enough for a monument, with room enough to pass
around it. We did, however, leave a small monument of loose stones
to mark this station, (station 35.) The thermometer stood at 33^ Fahren-
heit, which, with a steady breeze from the west, did not add to our com-
fort, especially as we had to confine our movements to such a small
area. While we were op here clouds began to come from the northeast
directly toward us and against the wind^ apparently moved by an under-
current, as they were below us. We could trace distinctly the track of
the slight snow which fell the last night, by it^s marks on the peaks of
the great mass. This peak was a spler«did point for a station, giviug
the key to the drainage and topography for miles around. To the east
and north the San Miguel and its tributaries appeared to us, from oar
RHooA.] GEOaRAPHY — ^EXPLORATION OF CANONS. 485
elevated standpoint, as if laid down on a map. Lizard's Head, a few
iniles east of us, formed a very prominent feature in the landscape,
althongh, looking at it Irom onr elevation, (14,280 feet,} its height did
not show. From this direction it ap[>ears quite broad, from the fact that
its greatest length is from north to south. To the west of us and quite
near was a pretty high mountain. Beyond it were scattered a number
of sharp, isolated pealcs, mostly under 13,000 feet in elevation, while still
farther to the west extensive plateaus reached to the horizon. In the far
aonthwest appeared several very dim, bluish mountains, probably con-
siderably over a hundred miles distant. Somewhat nearer to us, and a
little farther around toward the south, api>eared Ut« Peak, near the
southwest comer of Colorado. In the far northwest the Sierra La Sal
Mountains were distinctly visible. Much was also seen that has been
already described as having been seen from other stations. Mount Wil-
son is the highest mountain in Southwestern Colorado, and by far the
most massive.
The descent was made with great care, and, luckily, without accident
either to ourselves or the instruments. The descent over the snow bank
was much easier than the ascent, being accomplished by simply sitting
down on the snow and letting gravity do the rest. Below it, we found
several holes among the loose rocks, which bears had pawed out for
beds, but we met none of the animals themselves. We reached camp
quite early. The total height climbed on foot was 2,500 feet. It was
not very tiresome, but by far the most dangerous of all the climbs of
the summer.
After this we marched a short distance down the Dolores and made
stations 36 and 37. After that, returning by way of San Miguel Lake,
we recrossed the Bear Creek Pass, and camped at the creek junction,
where we had camped a week previous. The day after, we rode to
Howardville. We had scarcely got our dinner, when Mr. Jackson and
party came up from their trip to the ruins^ of which they gave glowing
accounts. On September 19 we started down tbe Animas, crossing,
over the southeast slope of Sultan Mountain, by the trail. We found
the trail very bad. At one point a tree-stump stood in it.
Some miners passing over this route a few days before had one of their
animals killed by its falling down the side of the mountain at this point.
The divide is about 10,400 feet in elevation, but the highest point of the
trail is several hundred feet higher. We camped near this latter point,
and the next dny left the train to follow the trail a few miles and
camp, while we rode in a southeasterly direction and made station 38,
on a rounded penk of quartzite, 13,046 feet in elevation. From h^re we
obtained the most striking view of the quartzite mountains. Tbe illus-
tration is reproduced from a topographical sketch made at tbis station.
The point is on tbe brink of the great Animas Caiion, which bere is
over 4,000 feet in depth ; a few miles farther down it is still deeper. Tbe
total length of the Grand Canon, from the mouth of Mineral Creek down
to tbat of Cascade, is about seventeen miles; below tbis, for about
seven miles, it becomes very narrow and straight, with a depth of about
1,000 feet. In returning to the trail we found the country terribly cut
lip along the head branches of Lime Creek, and even after reaching the
truil it was not tbe easiest we had yet had. Judging from what I have
heard and seen of the pass to the west of Sultan Mountain^ 1 think it a
much better route. Some fallen timber and swamp are encountered,
but not more than on tbis trail. We did not travel over it ourselves ; but
Mr. Jackson, who has been over both, gives the trail over tbe western
j^ass the preference. If ever a wagon-road can be built over into
I
486 GEOLOGICAL SURVEY OP THE TERRITORIES.
Baker's Park, from the sooth, it will be only by that way. The grroniid
is very rough along the trail to a mile or so south of the crossiDg of
(Cascade Creek, when it becomes more even, and the traveling^ t'ron
there on is very goo<i. Wagons could be brought this far, from the
south, without the least trouble. A long line of sandstone bloffis ex-
tends ])arallel to the trail for several miles, and rise from 1,500 to l,8(iO
i'eet above it. The trail passes along a sort of table, with these bloflb
rising above it on the west side, and th« Animas Gallon bounilin^ it oq
the east. Arriving at xluimas City, we stabled our riding-mules in a
deserted dwellingbouse, and, hanging up our instruments in another,
across the street from the first, made a thorough exploration of the
city. We found it located on a beautiful level pateh of ground, with
scattering yellow pines growing all over it. It was composed of one
street, with a row of log cabins on either side stretching a distiince of
several hundred yards. Some of the houses were nearly finished, some
half done, and the sites of others were marked by two or three tiers of
logs laid one above the other. All were deserted. We took posses^oa
of the best-looking one, which had a kitchen attached, and made our-
selves very comfoitable; eating inside and sleeping out of doors. The
night was so bright and clear that we could not endure sleeping under a
roof. We found several persons living in the vicinity, and from them
we learned that the settlers had been time and again ordered away by
the Indians, and had finally considered it best to leave. The height of this
place is 6,850 feet. From Baker's Park to this point, a distauee of aboat
twenty -six miles, the Aniinas has a fall of 2,550 feet, or an average of
100 feet to the mile. Trout are found in the river here, but how abun-
dantly I cannot say. They have never been caught as far up as Baker^s
Park — due, probably, to the falls between the two points.
Traveling dbwu stream, the stream-bed soon widens into a vexy
pretty valley, bearing the name of Animas Park. It extends from a
point near Animas City, so called, down the river about fourteen miles,
Avith a maximum width of two miles. The total area may be estimated
at twenty square miles, but the part capable of cultivation does not
amount to more than three or four thousand acres. The greater por-
tion of this can be irrigated at little expense. In parsing through it ire
saw corn, wheat, potatoes, turnips, and watermelons growing finely,
but all abandoned on account of Indian troubles. This valley is veiy
interesting in many respects. First it contains almost the only tillable
land within a hundred miles of the mines. Its distance from Baker's)
Park is only thirty-five miles by the trail. It is probably the richest
little valley in the Territory, and has an elevation of only 6,700 to 6,800
leet. It faces the south, and consequently is very warm, while at the
same time it is near enough to the mountains to get the benefit of their
great rain-fall. Near its lower end good coal is found in the greatest
abundance, while a plentiful supply of good pine timber is near at haod.
Farther down the river the country becomes a plain, almost perfectly
barren of vegetation. After passing through the park, we made sev-
eral stations, west of the river, on low hills. On station 45, which is
not represented on the accompanying map, but situated just a little
below the border, we found some old ruins, consisting of a couple of watch-
towers; one entirely disintegrated, leaving only a hole in the groand
to indicate its presence, while the other still remained about four feet
high, but was completely overgrown by oak-bushes. Some white and
painted pottery lay about. This point is a wooded hill, east of the Bio
La Plata. The day after, we found some pottery still farther north, on
station 46, which is on the map. After this we followed a road which
had been used by the former settlers, over to the Florida, and made
»HODA.J GEOGRAPHY — ^AKT£LOP£ PAKE, 487
BeTeral stations near tbat stream. The road soon ended, and we fol-
lowed its continuation, an Indian trail, to the Piuos River. This trail,
l>y an oversight, is not represented on the map. IMeavesthe Animasabout
lialf a mile north of station 46, and thence crosses over to the Florida,
^ivhich it follows up for several miles, then strikes across to the Pinos,
a^nd crosses that stream at the month of the Vallecito; crossing thence
over the next ridge, it strikes the Ute trail from Los Pinos agency. It
is not much used, and is m>i\» queutly qnite ditUcnlt to ioUow. There is
some line bottom-land on the Florida, capable of a high degree of cul-
tivation, but of small extent. Near the junction of the Vallecito aiid
Xfos Piuos is another small area of splendid land. These two streams
running down from thequartzite peaks, carry at least one-half more water
than any other streams of the same drainage area in the district.
The next day alter passing this |>oiut, October 2, snow began to fall,
and, camping near a peak on which we had to make a station, we qui-
etly waited for the weather to clear off. By a remarkable accident we
bad halted in a splendid camping-place, there being none worthy the
name for miles ahead of us, as we afterward found. Snow fell continu-
ously for four days, and we found sitting in camp very hard work. Ou
acconnt of our peculiarly protected position the snow that fell near our
camp melted as it fell, but a mile up stream it lay two feet deep. Had
it not been for the good grass and shelter here offered, our worn-out
mules would have fared badly. A thing worthy of note is the fact that
Tery slight thunder and lightning continued through the whole of this
snow-storm. Lieutenant Wheeler narrates a similar experience in this
part of the country. On the fourth day the weather cleared off, and
we succeeded in making our station, though on the summit the snow
was two or three feet deep, which, with our shoes nearly worn out, was
very disagreeable. Returning early from the peak we moved up the
ridge. The trail being entirely hidden by the snow, we had to give it
up, and after a very difficalt day's march we succeeded in getting out
of the snow only, and then had to camp in swampy ground, making
our beds on pine boughs, which we cut from the trees. We knew now
that winter had commenced, and we wanted to get out of the mount-
ains as fast as our mules could carry us. The next day we crossed the
divide at the head of Los Pinos lii ver, by way of the Ute trail. The pass
by this route was good, though covered with snow. In the summer it
must be very easy and i>leasant. We felt thankful when quite late in the
afternoon we reached the Kio Grande and struck camp near the wagon-
road. The next day we traveled down the road, which here is a ver^-
good one, to Anteloi)e Park, which we found to be quite an extensive
piece of plain country, forming here the valley of the Rio Grande, an<l
continued below, by a narrow s?trip of low land, along the river. The
elevation of the park is about 9,000 feet. There are several houses
dotted about over it and farms laid out, although the elevation is
too great to allow much grain to be produced. The next day, Oc-
tober 9, we ascended Bristol Head and made station 54. This is a
very curious bald mountsiin, a few miles east of Antelope Park, being
the southern culminating point of a high plateau. To the east it slopes
down quite gently, but on the west side it falls abruptly nearly 4,000
feet to the bottom of a very curious sink. In some places the bluff is
quite vertical for over a thousand feet. Beiug comi>osed of trachyte,
the rock breaks off along vertical planes and gives to the precipice the
character peculiar to volcanic formations. The sink already mentioned
is a little valley from a quarter to half a mile broad, bordered on the
east by the high bluffs of Bristol Head; and, ou the west, by a ridge
488 GEOLOGICAL SURVEY OF THE TERRITORIES.
and bliififs reaching seven to eight hundred feet above the valley. At
the lower end a narrow gate- way lends oat to the Eio Grande; and, at
the upper end, a beautiful lake occupies the highest part. Just above
this, Clear Creek cuts through the ridge on the west side, and flows oat
through Antelope Park. The whole mass of tliis basin has, aDdoub^
edly, fallen in; and, at one time, Antelope Park must have jutted up
against the side of the mountain. We made the ascent of the pe:jk
from the sink, riding our mules the whole distance, except the first part
of the climb, from the sink up to the ridge. On the summit we found
the snow about a foot and a half deep. A large be<ir had left his tracks
all over it. We found the slope to the east quite gradual and made the
descent on that side instead df going down the way we came up. After
camping at a point on the road to the south of Bristol Head, we moved
down the Itio Grande. The only place of special interest on the way
was Wagon-Wheel Gap, where the river passes for a few hundred yards
between two high bluiis, about 300 feet apart. This point has evidently
been, in times past, a great battle-ground between the Utes and their
enemies of the plains, the Che^i^ennes, Arapahoes, &c. Many little
heaps of rocks on the south blufl' seem to have done service as rifle-pits.
The toll-gate for the San Juan road is situated near this place.
We arrived at Del Norte on October 10. The town contains several
hundred inhabitants, and at the present time does a considerable basi-
ness with the San Juan mines. Leaving Del Norte we traveled across
San Luis Valley; far behind us we could see a new but apparently
greater storm than we had yet passed through gathering around the
distant mountains. Crossing over Mosca Pass and down Huerfano
Park we reached Pueblo October 18. The next morning we took the
cars on the narrow-gauge railway, and in the evening arrived at Den-
ver, our point of beginning.
METHODS USED IN DETERMINING THE ELEVATION OF
POINTS IN THE DISTRICT.
All the elevations given in this report depend upon readings of a
mercurial barometer. Where a standard barometer, whose elevation is
well determined, is within a short distance, this instrument gives a very
good determination of elevation. In the past summer, however, it was
quite impossible to establish a base barometer in the vicinity of the
region surveyed, without great expense. All the readings had to be
referred to distant stations. lieadings on high peaks were referred to
the Signal Service barometer on Pike's Peak, at an elevation of 14,U7
feet above the sea, while readings on all points under 12,000 feet were
referred to the barometer of the United States Geological Survey at
Fairplay, whose elevation is 9,904.5 feet. The first of these is one buu-
dred and iittyMniles distant in a straight line from the central part of tbe
San Juan country, while the second is one hundred and twenty-five miles
distant. These distiiuces are too great to give accurate results with the
barometer. At several points in the region we succeeded in getting two
readings at the same point at intervals of several days, but finding tbat
the resultingheights,as calculated by reference to those distant bases, did
not agree well enough, it was resolved to collect together all the data
possible from the field notes, and see if a fair trigonometric connection
between the mountain-peaks could not be established. The result was,
under the circumstances, highly satisfactory. It must be remembered,
BH0DA.1 METHODS FOR DETERMINING ELEVATIONS. 489
however, that these observations were not taken with the object in view
of making such a system of trigonometric levels. Moreover, the instra-
ment used read only to minutes of arc. Supposing an error of a min-
ute in a reading, which is not at all uncommon, the resulting error in
the dift'erenee of level of two peaks from a single observation will be
15.3 feet for a distance of ten miles and 23 feet for a distance of fifteen
mites. If, as is sometimes the case, the error be more than one minute,
the error in the elevation will be still greater. Another large and
uncertain element in the problem is refraction, which in the high mount-
ains is so changeable as to add much to the uncertainty of the results.
In many cases the observations were taken during storms, and often
the penks were sighted through breaks in the clouds, making the refrac-
tion still more uncertain.
From each station anglesof elevation ^or depression were taken to the
surrounding peaks and especially to previous stations. Had the fore
sights and back sights between the several stations been simultaneous the
erior of the refraction correction would have been very nearly neutralized,
but these two sets of observations were never taken at the same time,and
in only one case on the same day. From each of two stations I always
succeeded in finding some peaks which had been sighte<l from both.
With this material on hand the distances were obtained from Mr! Wilson's
plot of his secondary triangulation, which will not probably involve, in
any case used, a greater error than five-hundredths of a mile, which in-
cludes the error due to shrinkage of paper, as these distances were all
hastily taken off from the map with a scale. Having then the horizontal
distance between the two stations and the angle of elevation or depres-
sion from one to the other, of course the difference of level can be deter-
mined. But, on accoiui t of the errors which have crept into these angles
from the causes above mentioned, one determination of the differ-
ence of level is not sufficient. The back sight is then calculated, and
brings a different result. For a still finer approximation, wherever ver-
tical angles had been taken from the two stations to the same point,
the height of that above and below each station was calculated. From
this, another determination of the difference in the height of the two
stations was determined. Then the height of another uuvisited point
was calculated, and so on for all the near points sighted from both sta-
tions. Each point gives one determination of ihe difference of the two
stations. In some cases it will be found that one result is far out from
the rest. This may be due to the fact that sights to different points,
which have received, by mistake, the same number in the notes, have
been used. Such cases are thrown out, and a mean of the rest assumed
as the true difference of level. It was found that, on account of errors
of refraction and imperfections of the instrument, sights over fifteen
miles in length could npt be depended on at all. In the following calca-
lations no sights of that length were used, and in lact very few over ten
miles have been used.
In making the calculation, the following formula was nsed, taken from
Lee^M tabl(:*s *
dh = 0.00000485 K A ± O.0O0OO0C67 K»
In which dh is the difference of level of the two points, K the horizontal
distance in yards, and A the number of seconds in the vertical angle
nsed. In this formula are contained corrections for both curvature and
refraction, the latter element being assumed equal to 0.078 of the curv-
ature. On examining the notes carefully it was found that there were
sights to many hundreds of diiterent peaks, and it became a difficult prob-
lem to utilize all this material, and at the same time do it according to a sys-
490 GEOLOGICAL SURVEY OF THE TERRITORIES.
tern. After a number of experiments on different methods it was found
that to bring order out of this chaos, it was necessary to take up each
link in the chain separately, and use all the dat4). that could be found
pertaining to it, and determine the difference of level of these two sta-
tions finally. Next, the same process had to be gone through with the
line from the second point to the next station beyond, and so ou. In
doing this it was found that some of these lines were much better deter-
mined than the others. In finally reducing tbese differences of level
to a commou datum point, this fact might multiply the errors in the
work. For instance, a number of well-determined differences of level
might be transferred through a poorly determined line, thus vitiating
all with the error of the one. In order to obviate this the following
scheme was adopted: A central chain of well-determined lines was car-
ried through the heart of the mountain-mass from Mount Wilson, the
most westerly of the high peaks, to station 8, five miles east of Uncompah-
gre Peak, in the northeast corner of the mass. From this main line sev-
eral secondary branches were carried wherever the short lines could be
well determined. This system covered the whole mass of mountains.
Other stations, which could not be well enough determined independ-
ently, were connected with different [)oints in the main lines. In the
central line we have the following parts: From Mount Wilson testa-
tion 30, a peak east of it and distant 9.3 miles, is a fall of 383 feet, which
is the mean of five determinations having a range of 32 feet; thence
east to Sultan Mountain, a distance of 6.88 miles, with a fall of 536 feet,
the mean of six determinations, range 23 feet ; thence northeast to sta-
tion 16, distant 6.60 miles, a rise of 175 feet, the mean of nine determi-
nations, range 35 feet; thence northeast to Handle's Peak« 7.51 miles,
a rise of 456 feet, the mean of eight determinations, range 54 feet ; thence
north to Uncompahgre Peak, distant 11.14 miles, a rise' of 238 feet, the
mean of nine determinations, range 49 feet ; thence east to station 8,
distant 4.92 mi^.es, a fall of 1,380 feet, the mean of ten determinations,
range 67 feet. This completes the central or trunk line, whose length
is 46.35 miles. From Sultan Mountain a branch was extended eastward;
from this peak to station 25, distant 10.28 miles, a rise of 209 feet., the
mean of twelve determinations, range 67 ; thence to Rio Grande Pyra-
mid, distant 8.63 miles, a rise of 197 feet, the mean of nineteen determi-
nations, range 95.
From station 25, a branch extends to Mount Oso, distant 7.29 miles,
a rise of 64 feet, the mean of seven determinations, range 37.
From station 30 a secondary branch was extended south and west.
Station 30 to Engineer Mountain, distant 6.98 miles, a fall of 926 feet^
the mean of eight determinations, range 22 ; thence west to station 36,
distant 6.76 miles, a fall of 417 feet, the mean of eleven determinations,
range 51 ; thence to station 37, distant 3.65 miles, a rise of 94 feet, the
mean of tive determinations, range 35.
Another important sub-line extends from Sultan Mountain to the
northwest. The first link in the chain is the line from this point to
station 28. The heights of stations 30 and 16, above Sultan Mountain,
having been already well determined from the central chain, I made use
of all the connections between station 28 and each of these i>oints, re-
ducing all of them to a common point. The result from this was the
following: Sultan Mountain to station 28, distant 7.86 miles, a fjillof
484 feet, the mean of eighteen determinations, range 76 feet; thence to
station i 9, distant 3.77 miles, a rise of 324 feet, the mean of eight de-
terminations, range 43 feet; thence to Mount Sneffels, distant 5M
miles, a rise of 952 feet, the mean of six determinations, range 36 feet;
XHODA.] METHODS FOB DETERMINING ELEVATIONS. 491
tbeuce to station 34, distant G.G5 miles, a fall of 1,161 feet, the mean of
five determinations, range 23 feet.
This completes all the well-determined chains. Other stations on
which barometric readings had been taken, were connected with as
many points in the main lines as possible, and these being reduced to a
common point a mean was taken. Such points are the following:
Sultan Mountain to station 10, a fall of 223 feet, the mean of eleven
determinations, range 70 feet ; IJneompahgre Peak to station 5, a fall of
1,41>8 feet, the mean of ten determinations, range 85 feet. ITncompah-
gre Peak to station II, a fall of 3,024 feet, the mean of eight deter-
minations, range 111 feet; Sultan Mountain to station 51, a fall of 835
feet, the mean of three determinations, range 75 feet ; Sultan Mountain
to station 48, a fall of 1,001 feet, the mean of six determinations, range
59 feet ; Uandie's Peak to station 13, a fall of 1,175 feet, mean of fore
and back sights, range 6 feet.
Besides these there are two which depend on single determinations :
First, from Suit in Mountain to the point in Baker's Park where the road
crosses Cement (Jreek in Silverton, distant three miles, a fall of.
3,961 feet. Second, from Mount Snefi'els to station 32, which is obtained
from sights to a common point between them, distant from Mount
Snelfels 2.04 miles, and 1'rom station 32 3.75 miles, the fall is 5,050 feet.
This difiTereuce of level is checked by sights to distant points to the
south of station 32. Tljese two cases are admitted, because the distances
were so short as to preclude the possibility of any considerabl<^ error.
From all these results a table was made out, showing the heights of
each station above or below a common datum-point. Sultan Mountain
was selected as the datum i)oint, from its central location, and also from
the fact that it was sitnated on the great central chain of levels at its
junction with the two principal sub-lines.
A second column was added, giving the height of each station as deter-
mined by the single barometric reading laken thereon. A third column
was maile out from the first two by adding the number in the first
column to the one in the second when preceded by the minus sign, and
by subtracting it when plus. This column represents the elevations
above sea-level of Sultan Mountain, as determined irom the barometric
readings at the several stations. It will be seen that the twenty-three
results have a range of 203 feet. A mean of all these was assumed as
the true height of Sultan Mountain, and by reversing the previous
process and adding the plus diU'ereuces of height in the first column
and subtracting the minus, a fourth column was obtained, giving the
elevation of each station as reduced, from the mean of the twenty-three
readings. A fifth coluinn was added, giving the date of each reading
on the different stations. From this it will be seen that the observa-
tions extend from August 1 to October 6, more than two months.
By examining the table carefully, it will be seen that nearly all the
earlier readings give heights above the mean, and the later below it.
Whether this is merely accidental or due to some physical law, I cannot
tell. It will be seen that several of those stations, whose height relative
to the rest has been well determined, do not ai)pear in the table. This
is due to the fact that at those stations, either from storms or other
causes, we failed to get barometric readings.
492
GEOLOGICAL SURVEY OF THE TERRITORIES.
Name of station.
► 2 rt
0=0.2
'a) "fi ?5
Station 5 ,
Station 8 ,
Unconipabgre Peak . .
Station 10
Station 11
Station 13
Handie's Peak
Station 16
Rio Grande Pyramid
Saltan Mountain
Silverton ,
Stationer
Station 29
Station 30
Station 32
Mount Sneffels
Station 34
Mount Wil8on
Station 36
Station 37
Station 3H
Station 48
Station 51
I • • ■ • ■ •
Mean
-629
-511
-I-H09
-223
-2,755
-544
-f631
-f-175
4-407
0
-3,961
-777
-160
+531
-4, 258
+792
—369
+914
-812
-718
-320
—1,061
—835
43
qj ^ ■*»
<
12,770
12,9(i0
14,337
13,0^2
10,684
12,895
14,101
13, 593
13, 801
13, 29H
9, 377
12, 491
13, 120
13, 927
9,027
14, 162
12, 988
14, 185
12, 538
12, 623
13, 014
12, 321
12, 518
*» d
o
13,399
13,471
13,468
13, :«)5
13, 4:J9
13, 4:«
13, 470
13, 418
13,394
13, 298
13, 338
13, 268
13,280
13,396
13,285
13,370
13, 357
13, 271
13, :J50
13,341
13, 3:J4
13, 382
13,353
13,3C>6
12,737
12,855
14, 235
13, 143
10,611
12, 822
13,997
13, 541
13, 773
13,:)66
9, 405
12,589
13,206
13, 8ir7
9,108
14,158
12, 997
14,280
12,554
12, 648
13, 046
12, 305
12, 531
1874.
Aog. 1
" 6
" 8
10
12
14
15
17
22
31
31
Sept. 3
4
6
9
10
11
13
14
15
30
Oct. 6
«
It
ti
((
u
tl
It
u
«
It
<t
tt
It
((
•<
<l
if
With the elevatioDs of these stations determined, the heights of
unvisited points were obtained by applying the difference of level, as
obtained from the vertical angle, to the height of the station from which
the angle was taken. As most of the unvisited points are sighted from
many stations, we have for each a number of determinations of which
the mean is taken. Many of tbese points are quite as well determined
as some of the stations.
As it was impossible to connect all the peaks with the scheme of
trigonometric levels, it was thought best to give the heights of such as
nearly as it could be obUiined from the data at hand.
All these, it must be understood, depend on a single reading of the
mercurial barometer, not of the small aneroid. The latter instrument
was found to be worse than useless. Only one height depends on an
aneroid reading, that is Bear Creek Pass, but as here we had two differ-
ent sets of readings of three different aneroids, compared each morning
with the mercurial barometer, I thought best to put the height in the
list, but it must not be considered as very accurate.
In the following table are given, as nearly as may be, the heights of
all the peaks in the San Juan country above 13,000 feet, l>eside8 stations
and other points of interest. Some of the latitudes and longitudes have
been calculated, while the others have been taken from Mr, Wilson's
plot of his secondary triangulation, at a scale of two miles to one inch.
Some of these peaks being points of the primary triangulation, their
latitude and longitude will be more accurately determined when that
work is finished.
BHOOA.]
baker's park rectangle.
493
The first coloron in the table indicates the topographical designation
of each peak. The doable numbers indicate un visited stations. For
instance, 14 — 9 signifies the fourteenth peak sighted from station 9,
which .ever afterward bears that designation unless occupied as a sta-
tion. The term "Baker's Park rectangle'' signifies the projection rect-
angle included between latitude 37° 45' and 38° and longitude 107o 30'
and 1070 45', in which Baker's Park is situated. On the map the name,
by a sad oversight, was omitted, but its position may be known from
the fact that Howardville and Silverton are situated within it.
The absolute heights of the list may be out considerably, but the
relative heights are probably very near the truth. Whenever any point
in the system is well connected with sea-level either by a long series of
barometric readings or by a line of levels, it will only be necessary to
apply the trigonometric differences of height to obtain a very complete
and accurate table of elevations. It is proposed to make next summer
a connection with a standard barometer at Howardville.
BaJcer^s Fark rectangle.
Name or number of peak.
Station 17
8—17
Snltan Mountain
Mount Kendall..
10—16
11—16
8—16
6—14
Galena Mountain
Station 16
13—14
2—15
Station 27
12-9
11—9
Station 28
17—14
11—27
Handle's Peak...
2—10
Station 15
1—10
3—10
Station 29
3-8
5—26
8—5
5—10...
Station 10
1—5
12—10
57—9
13—10
14—10
21—1
10—10
Height above
the sea.
Latitude.
12.
13,
13,
13,
13,
13,
13,
1:^.
13,
13,
13,
13,
12,
13,
13,
12.
13,
13,
13,
13,
13,
13,
13,
13,
13,
13,
13.
13,
13.
13,
13.
13,
13,
13,
13,
897
390
366
rfc'O
300
030
400
450
290
541
4fc0
360
5^<9
770
830
882
390
630
997
440
675
720
770
206
480
120
200
787
143
2.-V0
4-20
120
490
OHO
970
010
o ' //
37 45 32
37 46 00
37 47 15
37 47 22
37 47 41
37 47 45
37 47 57
37 48 2
37 50 2
37 51 30
37 51 37
37 51 54
37 52 21
37 53 27
:«' 63 27
37 54 7
37 54 33
37 54 39
:^ 54 50
37 54 55
37 56 42
37 56 57
37 57 2
37 .57 24
37 57 50
37 58 12
37 58 27
37 59 30
37 59 40
37 59 47
.38 00 12
38
:J8
38
3S
38
1
1
1
3
4
Longitude.
16
17
46
42
52
o / //
107 33 30
107 36 8
107 42 2
107 36 51
107 37 30
107 38 20
107 35 47
107 32 32
107 34 8
107 37 10
107 39 8
107 35 48
107 41 58
107 31 49
107 31 18
107 41 10
107 36 24
107 44 52
107 30 4
107 37 6
107 33 20
107 32 3
107 32 48
107 41 58
107 29 35
107 41*11
107 35 11
107 44 48
107 35 39
107 30 20
107 44 23
107 37 5
107 44 6
107 43 49
107 30 30
107 31 52
494
GEOLOGICAL SURVEY OF THE TEEBITORIES.
East of Baker^s Park.
Name or number of peak.
Height above
tbesea.
Latitude.
LoD^tade.
Station 20 •.....•
19., 050
13, 274
13,656
13, 614
13, 5;w
13,815
13, 747
12, 822
13,967
14,004
13, 780
13,540
13, 700
13,600
13, 620
1.^, 520
13,660
10,611
12, 737
12,855
13, 510
14, 2:^
13, 670
13,080
o / //
:rr 46 58
37 47 7
37 47 52
:i7 48 54
37 51 34
37 51 58
37 54 40
37 55 27
37 55 80
37 56 36
37 56 56
37 57 17
37 57 24
37 57 52
37 57 55
37 58 28
in 58 53
38 1 34
38 2 00
38 3 16
38 3 57
38 4 21
:J8 6 27
38 7 21
O i 11
107 19 36
Mount Caobv .... .«..•• ........ .... .... ....
107 30 51
8t4]ktion 18
107 25 42
10—18
107 26 36
8—1
1«I7 %^ 57
12—1
107 27 54
10—13 '.
107 28 42
Station 13
107 28 15
Station 12
107 25 21
Ift— I
107 25 6
4—3
107 23 42
16—1
107 25 00
3—3
107 22 30
6—13
107 25 10
2—3
107 21 21
107 26 18
17—1
107 25 24
107 17 36
Station 5
107 14 24
107 22 18
14—5
107 29 38
107 27 32
24—1
107 26 44
107 27 18
West of Baker^s Park.
9—31
1—9
32—9
21—80
20—30
22-30
23—30
Station 30
6—27
4—27
5—27
Lizard's Head
Lizard's Head, base of column
7—27
Mount Wilson
1—35
4—9
8—27
3—30
2—30
9—27
10-27
Station 32
1—29
14—30
2-29
12— :10
Mount Sneffels
II— ;w
Station 34
13,120
13, 740
13,697
13, 377
13, 420
13, 730
13,180
13,897
13, 760
13, 170
13.400
13, 160
12, 8(58
13, 400
14, 2H0
14, 195
14,050
13,650
13, 690
13, 4c?0
13. 470
13,550
9.108
13,590
13. 810
13, 750
13, 730
14.158
13.500
12,997
o / "
37 44 54
37 45 27
37 46 00
37 46 6
37 46 15
37 46 47
:}7 47 42
37 48 2
37 49 28
37 49 33
37 49 34
37 50 13
ditto.
37 50 16
37 50 2:J
37 50 25
37 51 40
37 51 50
37 52 27
37 52 46
37 53 27
37 5:i 57
37 57 12
37 58 3S
XJ 59 20
37 59 26
:?7 59 38
38 0 17
38 0 36
38 1 54
//
107 51 51
107 51 31
107 49 23
107 47 18
107 46 58
107 52 7
107 52 54
107 49 SI
107 48 18
107 46 6
107 47 3
107 56 51
ditto.
107 47 12
107 59 18
108 00 7
107 58 54
107 46 31
107 48 22
107 49 41
107 45 7
107 45 oa
107 52 se
107 47 W
107 49 15
107 47 58
107 50 48
107 47 21
107 51 33
107 54 23
BHODA.]
ELEVATTOKS.
495
Quartzite Pedks^ south of Bdke^^^s ParJc.
Name or number of peak.
Heij^ht above
the sea.
Latitude.
Longitude.
Station 48 ..-.
12, 305
13,650
13,000
13, 275
13,110
13,380
13, 640
13, 630
13, 180
13,800
13,580
14,054
14, 054
14, 033
13,728
13, 928
13, 746
13, 78:j
13, 560
13, 680
13,1(K)
13, 600
13,580
13.6rj0
13, 700
13,800
13, 750
13,730
13, 831
13, 800
13, J>40
13,046
o / //
37 29 20
37 34 55
37 34 57
37 35 12
37 35 48
37 35 52
37 36 29
37 36 31
37 36 41
37 36 48
37 37 9
lYT 37 21
37 37 24
37 37 43
37 37 43
37 38 2
37 38 40
37 38 49
37 39 52
37 39. 52
37 39 54
37 40 18
;f7 40 19
37 40 27
.37 40 43
37 40 52
37 40 57
37 41 12
37 41 27
!^7 41 42
37 41 56
37 41 59
O 1 II
107 35 56
9—23
107 28 42
21—31
107 40 18
10—23
107 29 6
11—23
107 30 18
8—23
107 29 2
Monnt Oflo ......
107 29 25
9—21
107 34 24
13_23
107 27 25
1—23
107 34 44
2—23
107 32 59
7—9
107 35 21
Mnnnt iTJolnH..,,,, ,,,»., ,.r,,. t ^ r
107 :i7 12
8—9
107 35 32
Pidseon'a Peak .............................
107 :J8 16
107 38 36
10—^^1
107 37 27
11-21
1—14
5—23
107 34 51
107 32 14
107 35 18
1—38
107 43 22
5—14
107 34 36
107 32 42
4—14
107 34 00
3—14
107 a3 24
12—14
107 35 18
9—14
107 34 47
16—14
7—14
107 35 22
107 35 56
8—14
107 36 25
4—17
107 33 18
Station 38
107 41 20
Southeast of Baker^s Park.
Station 51
Station 22
11—17
10—17
12—17
Rio Grande Pyramid
3—18
9—17
Station 24
2—18
7—17
8—17
14—14
12,5.36
13,020
13, 090
13, 200
13, 170
13, 773
13, 220
1.3,090
12, 9i37
13,210
13, 310
13,260
13,430
o / "
37 29 52
37 36 6
37 39 38
?7 40 38
37 40 39
37 40 50
37 41 24
37 41 20
37 41 46
37 41 55
37 42 14
37 42 16
37 42 47
O I II
107 22 24
107 23 48
107 29 11
107 29 40
107 :jo 15
107 23 21
107 22 17
107 29 57
107 29 55
107 21 56
107 28 38
107 29 29
107 27 18
496
GEOLOGICAL SURVEY OF THE TERRITORIES.
MUcellaneous elevations.
Xame or namber of peak.
Height above
tbeaea.
Latttnde.
1
Lonfptade.
1
o
/
It
o
/
ti
13, MO
37
58
12
107
4
3
12, 670
38
7
42
107
12
35
9,100
38
16
48
107
9
6
12, 971
37
42
4
107
48
12
12,554
37
42
48
107
55
37
12, 648
37
41
19
107
14
11
10,613
37
35
12
107
49
55
10,580
37
25
40
107
55
42
8,100
37
16
45
107
49
20
8.300
37
11
18
107
59
24
8,930
37
19
35
107
42
15
12,800
37
47
'15
107
3
6
9,700
37
50
12
107
35
42
9,400
37
48
48
107
39
40
12,540
12,090
10,460
11,570
11,098
12,600
'
10, TOO
""""• ~
Station 2*
Station V
Station ?•
Eugiueer Mountain
Staiiou 36
Station 'S7
SrationW
Station 4-i»
SUtion 44*
Station 45**
Station 47*
Bristol Hea<l* ,
Howanl ville
Silverton .•
Lake Fork Pass*
Cnnningham Pass*
Pass east of Sultan Monnt*
Pass west of SnUan Monnt* ...
Pass at head of Mineral Creek*
Bear Creek Pass (a)
Weminuche Puss*
The Atar denotes points whose hei<;hta depend ou a single reading of mercurial barometer,
(a) Height determined by aneroid barometer.
NOTES USEFUL FOR THE LOCATION OF MINERS' MONU-
MENTS IN BAKER'S PARK.
m
Salt<an Monntain is tbe peak at the south end of Baker's Park. In
the following notes the monument built by this party on the southern
knob is used as the station. Station 16 is a high massive )H$ak, two
miles northwest of Howardville, but not quite visible from the town ;
it may be seen from a point a little up the side of Galena Mountain.
On the summit we left a small monument of stones. The latitude of
station 16 is 37o 51' 30".5, and its longitude 107o 37' 9".8. The latitude
of Sultan Mountain is 37° 47' 16", and its longitude 107^ 42' 1".5 ; at
station 16, Sultan Mountain bears south i2P 11' west ; at Sultan Monnt-
ain, station 16 bears north 42^ 8' east. The distance between the two
points is 6.60 miles. By using this as a base any engineer can locate ac
curately a monument at any point visible from the two stations. Silver-
ton and the whole lower end of the park are visible from both points,
as well as points on the side of Galena Mountain, and also others near
Arustra Gulch.
Declination of magnetic needle.
Locality.
Station 11
Bio GraDde Pyramid
Station 30
Engineer Mountain
Station 32
Station 34
Mount Wilson
Station 36 s.
Station 37
Doclination.
E. 150 i.v
E. 12° 56'
E. 8o ny
E. 13° 56'
E. 15° 5^
E. ICO 55/
E. 130 8'
E. 16° 15'
E. 140 23'
Date.
1874.
Anguet 1)
Anfjrnst 9i
September 6
September 7
September 9
September 11
September 13
September 14
September 15
GENERAL INDEX.
A.
Pago.
Alkali lands 260
AUnviam of Nebraska 256
Amphitheatre Mouotain 70
Analyses of coal - 175,176,177
Loess deposits....' , 246
Missouri River sediment 252
soils of Nebraska 258,261
Ancient lake-basins of the West *..... 47
ruins in Southwestern Colorado 369
Andrew,Prof. E. B 279
Animas Caflon 486
City 486
Forks 229
Park 219,476,486
River 206,369
fall of, from divide to lower end of Animas Park 446
Antelope Patk 199
Anthracite coal 67,176,177
Creek 98,99,138,176
Arastra Gulch 230,466
ArchsBan rocks of Eagle River 106
Grand River 107
Gunnison River ,... 107
Arkansas marls 52
River 47,48
morainal deposits 47
Ascent of Mount Snefifels 479
Aspen Creek 66,69
Angbey, Samuel, Ph. D., report on superficial deposits of Nebraska 243
Avalanche Creek 62
Aztec Springs 377
ruins 378
B.
Bad lands of Nebraska 261
Baker's Park 206,230,464
rectangle 493
Basalt. 163,198
Basaltic areas 178
Bear Creek 206,217,477
Pass 477
River group 144,145,154
Bellevue Mountain 419
Big Casino lode 2:^6
Bitter Creek series 145
Black Butte 291
Blue Creek 97
River 65
Bluff country 193
Bradley, F. H 111,112
Breccia •••• 156
trachytic 200
Bridger group 140,149,156
Bristol Head 206,469
497
498 INDEX.
c.
Calciferons rocks Ill
of Eagle River 113
Grand Kiver 113
Canadian period Ill
Ca&un of Eagle River 81
Grand, of Gannison 97,425
Unaweep 94,104
Capitol Peak 55,ti6,417
Carboniferous age 114
beds and strata (>l,66, 81.214
coal-measures 117,281
fossil flora 27d
group 42
rocks of Eagle River 114
Grand River 116
sections 115,116
Caclcade Creek 215
Castle Peak 66,418
Catalogue of minerals 178
rocks fc 179
Oanseof peculiarities of Loess deposits in Nebraska 248
CeboUa Creek 97
Cedar Creek 103
Cenozoio formations 140
Chittendon, George B 5
Cinnamon Mountain 419
Clifl-houses at Rattlesnake Bend 373
in Mancos Caiion 371,373
Coal 67,99.139,175
analyses of 175,176,177
table of comparison 177
anthracite 67,176,177
beds, Cretaceous 226
Creek 99
measures, Carboniferous 117,5281
Cochetopa Creek ^ 94
Colorado group 45
range , 37,45
geology of 41
Springs, geology of 41
Comparisons of aneroids with mercurial barometer 447
Comstockiode ,. 234
Prof.Theo 111,124
Cope,E. D 13,16,145,150
on the Lignitic group 153
Monument Creek group 37
Triassic in New Mexico 42
Creek, Anthracite 96,99
Aspen 66,69
Avalanche 62
Bear 217
Blue 97
Cascade 215
Castle 57,60
Cebolla 97
Cedar 103
Clear 58
Coal 99
Cochetopa 94
Frying Pan 87
Godwin 204
Junction • 221
Kahnah 105
Lake 48
Lime 210
Maroon 57,60
McElmo 378
Mesa 91
.
INDEX. 499
Page.
Creek, Mineral 217
Moantain 97
North Mam 89,90
Oh-be-joyfal - 176
Ohio 94,95
Pine 22
Piney 81
Plateau 89,91,421,423
Roche Montonn^e 80, HI, 83
Eock 59,61,63,65,69,68
Roubideau's 104
Sopris 60
Teocalli : 70
Vallecito 216
White Earth 202
Cretaceous beds 55,57,60,61,64,65,69,86,87,89,90,97
division of 128
flora 284
of Greenland 321
North America .-. 316
^onp ...^ 45,128
m New Mexico 129
Lower i-. 128
Middle... 135
No. 1 (see Dakota group.)
No. 2 135,224
No. 3 135
No. 4 : 137,139
No. 5 137,139
Cunningham Gulch 229
D.
Dakota group 45, 64, 67, 69, 82, 87, 88, 96, 97, 101, 105, 128, 284, 292, 316, 321
evidence of age of 128
fossils of 128
in Arizona 134
of Eagle River 129
Grand River 130
Gunnison River 130
sections of 131,132,133,134
Daly, Mount 66,418
Dawson, G.M 152,286,287
J.W 287
Declination of the magnetic needle 49t^
Description and enumeration of Cretaceous plants 333.
Devonian age 114
fossil flora 277
strata 115,211
Dikes 55,99,100
Discussion of use of aneroids 447
Distribution of vegetation 428
District assigned middle division 415
Divide between Grand and Gunnison Rivers 92
Dolores River 206,215,370
Dolerite 198
DrlTb of Nebraska 243
E.
Eagle River 79, «1, 84, 161, 171, 421, 433
Archaean rocks of 110
Calciferous rocks of 113
Carboniferous rocks of 114
Dakotagronp on 129
Jurassic rocks of >. 124
Middle Cretaceous of 135
Permian rocks of 118
Primordial rocks of 110
rate of fall of 433
500 INDEX.
Page.
Eagle River, Triassic rocks of 122
East River 95
Ecooomical geology - 175
Electrical phenomeua 466
Elevations 429,492,494,495,496
of junctions of streams 433
monntains 441
parks, valleys, &c 442
passes and divides 443
on White River plateaa /42
revision of, in Elk Moantaip 430
Sa watch range 429
Elk Mountain range. ..^ 54,64
geology of 54,58
northwestern portion 59
Mountains 92,100,416
elevations of .- 4:M)
revision of elevations in 430
Endlich, F. M., S. N. D 103,114,124,139,152
letter to Dr. Hayden 183
report of 181
Engineer Mountain 207,217
Erosion 161
Eruptive rocks - 163
Excelsior lode ....^ 235
F.
Fault-fold of Elk range 68
Florida, Rio 224
Fort Benton group 135
Pierre group 137
Union group 23, 141
Fossil flora of Carboniferous 278
Cretaceous 284
Devonian 277
Jurassic 283
Triassic 283
plauts of Liignitic group 32
Silurian group 276
Fossils of Permo-Carboniferous 118
Fox Hills group •. 35,45,137,139
Fremont, Capt. J. C 415,416
Front range 37,45,436
Fruit on the Loess deposits 249
Frying Pan Creek 87
Fuel fiom surface-deposits of Nebraska 262
G.
Oallieteo sand group 150
Gannett, Henry, M. E., geographical report of 413.
Garden of the Gods t 43
Gauging of streams 440
GeographicaL report of Henry Gannett 413
Geography. ..« 411
of middle district, etc 416
Geology of district drained by Rock Creek 63
eastern base of Colorado range 40
Pleasant Park 41
Sopris Peak and vicinity 61
Gilbert, G.K 162
Gill, Theo., letter to A. C. Peale ..' 153
Glacial action *. .,.49,161,192
Godwin Creek 204
rate of fall of. 447
Gold 175
Golden City 33
Gothic Mountain 55,419
Grand River 57,85,93,101,172,421,437
INDEX. 601
r
Grand River, Arcbsban rocks of 107
Calciferous rocks of 113
CarboDiferous rocks of 116
Dakota group of 130
Jurassic rocks of 125
Middle Cretaceous of 135
Pernjian rocks of l^O*
Primordial rocks of Ill
rate of fall of 432
Granite 66,68
of quartzites Ib9
town of 51
Great Amphitheatre 206
Plateau 420
Green Mountain lode 2i}4
River group 140.147,156,159
Gunnison cattle-camp ^ ^ 95
Cafion 97,425^
Capt. J. W 415
City 95,435
River 94,161
Aroba>an rocks of 107
Dakota group of 130
Jurassic rocks of 126
Lake Fork of 94
Middle Cretaceous of 135
North Fork of .- 93,94,98,101,427
rate of fall of 433
Smith's Fork of 94,97
Valley 42a
Gypsiferous beds on Eagle River 83, 119
Grand River 120
Gypsum 178
II.
Hall, Prof. James .• 276,278
Handle's Peak 190,204,460
Haydeu, F. V 100,117,121,126,145,150,178,285
letter to the Secretary of the Interior 1
on Jurassic 124
Potsdam sandstone Ill
report of 19
Highland Mary lode 23:J
Higlev's mine 34,38
Holmes, W.H 7,48,100,126,178
report of 59
Holy Cross Mountain 54,55
Hopkins mine 33
Hoven weep Valley, ruins in 381
Howardville 465
I.
logersoll, Ernest, letter to Dr. Hayden 385
report of 383
Inscriptions near cliff-houses 375
Introduction to report of A. C. Peale * 77
T. M. Endlioh 185
Intrnsfon of volcanic rocks 219
Italian Peak 418
J.
Jackson, W. H 11
on ancient ruins in Southwestern Colorado 360
report of 367
Junction Creek 221
Jurassic flora 283
group 44,124
in Elk Mountains 57
rocks 60,70,97,105
sections of 61,125.126,127
502 INDEX.
E.
Kaboab Creek
King, Clarence, map referred to,
L.
Lacustrine deposits of Nebraska, origin of ^30
Mollusksin 266
Ladd, S. B., M. E., report of 435
Lake Creek 4^
Fork of Gannison Biver M
rate of fall of 447
Lower Twin 49
San Cristoval 203,455
San Miguel 228,477
La Plata group 208
Latitudes 432
Lead ^ 175
Leidy, Prof. Jos 21,24,140
Length of Loess age in Nebraska 253
Lesquereux, Leo 15,21,118,128,140
LesquereuZ| Leo, letter to Dr. Hayden 273
on fossils from Carboniferous strata from Ca&on City 42
reportof 271
Letter of A. C. Peale to Dr. F. V. Hayden 75
Ernest IngersoU to Dr. F. V. Hayden 385
F. V. Hayden to Secretary of the Interior 1
Henry Gannett to Dr. F. V. Hayden 413
Leo Lesquereux to Dr. F. V. Hayden 273
8. B. Ladd to Dr. F. V. Hayden 4:55
W. H.Holmes to Dr. F. V. Hayden 69
Life of Loess age in Nebraska 254
Lignitic group 20,24,26,29,30,33,34,44,140,152,275,289
at Canon City 28
conclusions in regard to • 35,155
fossils of '. 32
history of 19
sections of 30,31,33,34
Lime Creek - 210
List of authorities on Mollusca 407
localities of Mollusca 386
Little Giant lode 235
Lizard's Head 207, 476, 483, 4»
Lode, Big Casino 236
Comstock 234
Excelsior 235
Green Mountain .• 234
Highland Mary 233
Little Giant 235
Ouray 236
Pelican 236
Pride of the West 234
Prospector 236
Robert Bruce 234
Yreteva 2M
Lodes, age of 237
occurrence of 232
origin of ' 238
Loess age, length of 253
life of 254
deposits of Nebraska 245
analyses of 236
causes of peculiarities 243
fruit on 249
scenery of 250
Longitudes 432
Los Pinofl Indian agency 95
Rio 446
Lower Cretaceous 128
Twin Lake 49
1
INDEX. 503
M.
Page.
Mallett, Professor 67
analysis by 177
MancosCa&OD, cliff-houses in 373
ruins in 370,373
tower in 374
Rio^elos 369
Manitou •. 44
Marcellina Mountain 99,166,420
Marcou, Jules 124,127
Maroon Mountain 66,418
Mai-vine, A.R 1,83,83,87,107,111,114,120,124,139,152
McElmo Creek 378
Means of communication between Denver and San Juan country 443
Medicine Bow Mountains 436
Meek and Bannister 285
Meek and Uayden 117
Meek,F.B 15,139,145,152,212,279
on Silurian strata of Canon City 41
Mesa Creek -... 91
Verde 369,370,378
Mesozoio formations 121
Metamorphic area 187
rocks 106
Methods used in determining elevations of points in San Juan district 488
Middle Cretaceous 135
sections of 136
Middle Park 85
Mine, Higley^s 34
Hopkms 33
Mineral Creek 217
Point 233
Mines, San Juan 229
Mollusca, list of authorities on 407
special report on 388
MoUusksin Lacustrine deposits 266
Monument Creek group 36,37,150
Moraines 49,51,52,53
Mount Daly 66,418
Italia 55
Lincoln 48
Marcellina , 99,166,420
Oso 188
Sneffels 205,479
ascent of 479
Wilson 207
Mountain, Amphitheatre 170
Bellevue 419
Cinnamon 419
Creek 97
country 193
Engineer 207,217
Gothic 55,419
Holy Cross 54,55
Maroon 66,418
Snow Mass 55,66,418
Sultan 217
Teocalli 70,419
Treasury 65,419
West Elk 65
White Bock 55,66,70,419
Mountains, Elk 54,59,92,100
Medicine Bow 436
San Juan 452
N.
Nebraska alkali lands 260
badlands 261
sand-hills 259
504 INDEX.
Nebraska, snperflcial deposits of 243
water-resoarces of 863
Newberry, Dr. J. S 14,21,24,122,152
on Cretaceous of New Mexico - 129
Dakota group of Arizona 1^
Jurassic 127
Potsdam saudstone of Colorado River Ill
White River group 25
Niobrara division of Cretaceous 135
Notes useful for location of miners' monuments in Baker's Park 496
Nortli Fork of Gunnison River 9o 98,101
Main Creek ' 8i>.90
Park 436
O.
Oh-be-joyful Creek 176
Ohio Creek 94,95
Origin of Lacustrine deposits in Nebraska 250
Oso, Mount 1««
Ouray lode 236
P.
Painted Desert of Arissona 127
Paleontology 271
Paleozoic tormations . 110
rocks 61,63,70
Park, Animas 219,486
Antelope 199
Baker's 206,230,464
Cone 419
Middle 85
North 436
Range 48,436
Pass, Bear Creek 471
Tennessee 47,52
Passes, elevation of 442
to Baker's Park 465
Peale, A. C 00
on Carboniferous strata of Eagle River 42
letter of, to Dr. F. V. Hayden 75
report of 73
on thickness of Red beds in Pleasant Park 4^
Peak, Capitol 55,66,417
Castle ^ 66,418
Handle's 190,204,460
Italia 418
Pyramid 418
Sopris 55.66,417
Uncompahgre 204,452,453
Pelican lode 236
Permian fossil flora * 281
strata 80,117
section of 119
Permo-Carboniforous strata 117,118,119,120
fossils of 118
Pine Creek 52
Piney Creek 81
Plateau Creek 89,421,423
country 193
Plateauf*, elevations of 433
Platteville 33
Pleasant Park 43,44
geology of 41
Point of Rocks 155,285,287
fossil plants 286,289
description of 296
Porpbyritic trachytes 163,165
Post-Tertiary formations 161
IKDEX. 505
Page.
Potsdam group 80,110
of Eagle River HI
Grand River Ill
Previoas explrratioDs of middle district 415
Pride of the West lode 234
Primordial period , 110
Prospector lode 236
Pront,H. G. 416
Psendomorphs after salt 212
Pyramid Peak 418
Rio Grande 198,200,470
Q.
Qaartzite monntains -. 187,473
Qaebec group 111,112
B.
Kaiige, Elk Mountain 54,58
Front 37,45,436
Park 48,436
Sawatch 48,54
Wasatch 47
Rattlesnake Bend 374
cliff-house at.... .' 375
Red beds 42,57,86,97
age of 121
stratum 197
Boportof A. C. Ptale 73
A. D. Wilson 443
Ernest IngersoU - 383
F. M. Endlich, S. N. D 181
conclusion of ....^ 239
Franklin Rhoda 451
F. V. Hayden 19
Henry Gannett 413
Leo Lesquerenx 271
Samuel Aughey, Ph. D 241
8. B. Ladd 435
W.H.Holmes 59
W. H. Jackson 1 367
on northwestern portion of Elk Mountains 59
natural history 385
Reports of Henry Gannett, S. B. Ladd, and A. D. Wilson 411
Review of Cretaceous flora of North America 316
Rio Animas 206,369
rate of fall of 446
delosMancos 369
Dolores 206,:«'O
Florida ' 224
Grande del Norte 198,370
rate of fall of 446
Pyramid : 198,200,470
La Plata 369
Los Pinos, rate of fall of 446
San Juan 369
Miguel 206,216
River, Blue m , 85
Dolores 7 :...206,315,370
Eagle 81,84,421
East . . 95
Grand .".".V.V.V.V.V.V.V-V.V.V.V.V. !"."!!! I HI ."! Ill ."."". I .".'.".' ." ." ." .'57,'85.'93, 421, 437
Gunnison 94,424
North Fork of 93,98
Mancos 369
Slate 94
Uncompahgre 94,103
White 437
Yampah 437
Roads 428
506 INDEX.
Roads SDd trails 4^
Eoaring Fork 56,66,86,88,422
rate of fall of 433
synclinal 59
Robert Bmeelode «.... 234
Roche Moatonn^e Creek 60,81,83
Roches Montonn^es 161,192,230
Rock Creek 59,61.63,65,69
Rogers, Prof. H. D 2el
Roubideaa's Creek 104
Ruflfner, Lient. E. H 98.99,416
Rains at Aztec Springs 3/#
in Mancos Ca&on 373
on the Hovenweep 381
McElmo 378
Rhoda, Franklin, report of 451
Rhyolite 197,204,206
S.
Salt Mountains 103
San Cristoval Lake 203,455
San Juan City 199
mines 229
Mountains 452
River 369
San Mignel Lake 223
River 206,215,477
rate of fall of 446
section on 227
Sand-hills of Nebraska 259
Sawatch range 49,54
revision of elevations of 429
Scenery of Loess age in Nebraska 250
Schimper, Professor 279
Sedimentary area of San Juan district 210
Settlements >. 428
Shumard, Ur. G. D 117
Sierra La Plata..-. 369
LaSal 103
San Juan 309
Silurian age 110
formation 210
fossil flora 276
strata in Eastern Colorado 41
Elk Mountains 57,69
of Eagle River 113
section of - 113
tables of comparison of 112,114
Silver 175
Silverton 465
Slate River 94
Smith's Fork of Gunnison River 94,97
Sneffels, Mount 205,479
ascent of 479
Snow Mass group 65,^
Mountain 55.66.418
SoprisPeak 55,66,41
geology of 61
Special report on Mollnsca 389
Strata, sections of, 30. 31, 33, 34, 38, 102, 113, 115, 116. 118, 119, 122, 125. 126, 127, 130, 131.
132, 133, 134, 130, 137, 138, 156, 169.227
Saltan Mountain 207,217
Superficial deposi ts of Nebraska 24:1
fuel from *, 268
Swallow and Hawn on Permian strata 117
T.
Table of analyses of coal 177
Bear River group 144
Bitter Creek series 145
INDEX. 507
Page.
Table of Bridijer group 149
Fort Uniou group 141
Green River group 147
relations of fossil plants of Point of Rocks 286
subdivisions of Tertiary of Europe 284
Wasatch group 147
White River group 150
Wind River group 148
Tables of Tertiary strata 23,151
Tennessee Pass 46,47,52
Teocalli Creek 70
Mountain 70,419
Terraces 161
Tertiary flora of North American Lignitic as evidence of the age of the formation 275
fossil plants, new species of, described 308
strata 140,156
tables of 23,151
Timber in modern geological times * 265
Topography and geography 411
Topographical report of S. B. Ladd 4'\^
San Juan country 451
Tonsland 33
Tracborheites 163,168
Trachytes 163
classification of 195
Trails 428
Treasury Mountain 65,459
Triassic flora 283
group • 42
strata 70,97,105,121
of Eagle River 122
Grand River 123
Gunnison River 123
sections of 122
U.
Unaweep Gafion 94, 104
UncompahgrePeak 204,452,453
River 94,103
rate of fall of 446
Valley 424,453
Upper Cretaceous 137
sections of 137,138
V.
Vallecito Creek 216
rate of fall of 446
Vegetable organisms of uncertain affinity 363
Vegetation, distribution of 428
Volcanic area, San Juan district 193
rocks 219
W.
Wagon Wheel Gap 199
Wasatch group 147,158
range 45
Washakie group X46
Water-resources of Nebraska 263
West Elk group 65
West, H. T, appendix to chapter 2, report of F. V. Hayden 38
White Earth Creek 202
River 4:j7
barometric base 436
group 24,25,150
fossils of 25
plateau 437
Rock Mountain 55,66,70,419
508 INDEX.
Paft
Wilson, A. D.. report of 443
Mount 207,4S3,4?S
Wind River groap 148
Y.
Tampab River 437
Yretevalode 234
Z.
Zoology 3S3
INDEX OF SYSTEMATIC NAMES.
Page.
Abietitcs ErnestiDSB 334
AceracetB 359
AceresB >, 332
Adiantites 278
Aescnlns antiquas 289
Affriocbanis 25
Alethopteris 280
Alnites nniequilateralis 307
Aluns KeforsteiDii 293
AmeDtaceso 339
Ammonites • ' 29,35,56
lobatos 30
pericariDatus 129,134
AmnicoliDie 390
Ampelideo) 352
Ampelophyllnm 354
attennatam 354
ovatam 355
Ancbitberinm 23,25
AncylinsB 405
ADcylas parallelns 405
Andromeda afflnis 348
parlatorii 348
Anisopbyllnm semi-alatnm 363
Annularia 276
Anomia 34
AqnifoliacefiB 359
Aralia 138
concreta,. 349
qQinqnepartita 349
oaportanea 350
Towneri 349
tripartita 348
Arcbeopteris ; 278
Aristolocbites dentata 347
Arteropbyllites gracilis 279
Artiodactyle 37,160
Arundoobtasa 311
reperta 311
Asapbos 112
AsarineiB 347
Aspidiopbyllnm trilobatam 301
Atbyria ; 213
Bubtilita 216
Avicnla 115
lingnaformis 137
Avicniopecten 115
Baculites 29,35,56
ovatna 30
Bakevellia 115
Batbynrus 112
Belleropbon 213
Betala beatrloiana ?... 339
Vogdeeii 312
Btcornea 348
Calamites 42
gigae 118
Suckovii 118
509
510 INDEX OF SYSTEMATIC NAMES.
Canis 23,25
Oardiocarpon Soathwellii 279
Cardiom speciosum 35
Carpinas p^andis 313
Carpitesvibarni 308
Carpolithes 279,289.364
Castanea intermedia 313
Caator 23.25
Ohioensis • 263
Canlinites spinoea ,..» 361
Celastrophyllum ensifolium 'SjQ
Cervas 25
Chseropotamas 23
Cinnamomam Miasissipiense 291
Cissites 352
acuminatus 353
affinis 352
cyclophylla 353
HarkerianoB 352
Heerii 353
obtasuin 354
Cissas parottiffifolia 314
Clathropteris 134
Colamniferesd 332
Compsemys 23
CoDchifura 406
Conifers 334
Conocoryphe 112
Corbicala 22,23
CorbicuiadsQ 406
Cordai tea principalis 42
Crinoids 114,211
Crocodilas 23,158
Capalivierae i 340
CycadeaB 283,334
Cyclopteris 134.273
Daphnogene cretacea 343
Heerii 343
Dictionema flabelliforme 276
Dimyaria *. 406
Diospyros ambigna 348
brachysepala 306
f ficoidea 314
rotuudifolia 348
Discorea f cretacea 338
Discoreas 338
Dombeyopsis obtusa 32
Dryophy Hum oi*enatam 301
(Quel ens) latifolium 340
primordiale 340
saMcifolium 340
subfalcatnm 340
Elephas , 25
Americanos 251
Embothrites daphneoides., ^ 347
Emys 23,25,158
EBtelodon....- 25
Equihetnm 216
Equus 23,25
Eremophyllum fimbriatum 363
Euomphalus 112,213
Fagus polyclada 341
Felis 23
Ferrea stern bergii 139
Fious asarifolia 303
dalmatica 303
distorta 342
Halliana 341
irregularis 304
INDEX OF SYSTEMATIC NAMES. 511
Page.
Ficus laurophyllam 342
ovalis r 313
plaDicostatu 291,304
pseudo-popalus 313
tillffifolia 32,291,304
Wjomiogiaua 314
Fillices 333
Flabellaria? minima 338
Frangulacesd 360
Fucus lignitum 296
Gamopetalesa 348
Gasteropoda 22,390
Gieichenia KarriaDa '. 334
Nordenskioldi 334
Glumacese 338
Glyptostrobosgracillimns 337
Goniopteris puTchella 309
Greviopsis Clebami 291,306
Haydenii 359
Grypbaea pitch<jri 129,134,224,226
Halymeuites , 31
Hamamelites Eansaseana 355
qnadrangulariB • 355
Hedera ovalis 351
platanoidea 351
Scbimperi 351
Helicidro 392
HelicinsB 396
Helisonea plexata 402
trivolvis 404
Helix 23,25
Leidyi 24
(Micropbysa) iDgersoUii 397
Hipparion 25
Hya)uodoii 23,25
HymeDopbyllites 280
Hymenophyilum cretaceum 333
Hyopotamus .25
Hypaam Haydenii 309
HyracodoD 25
Ilex strangulata 359
IncertsD s^is 361
luoceramus 29,30,35,56,136,224,226
barabina 137
Crispii 129,134
iDolepis 337
Iscb^romys 25
Iteoidete » 338
Juglans alkalina 308
Debeyana 360
rbamnoides 307
rugosa 291
Jnniperus occidentalis • 86
Lamellibranchiata — >- 22
Laurinese 327,342
Laurus macrocarpa 342
(Persea) prcestansf 305
proteififolia 342
Legnminusites altemans 315
Lemnascutata 287,288,:i00
Lepidodendron carinatnm 279
modulatam 279
Lepidotns 23,24
Leptancbenia 25
LeptocbcBras 25
Leptomeryx 25
Limax castaneiis 396
moDtanuB 394
Limnsea 23, 2&
512 INDEX OF SYSTEMATIC NAMES.
LimnsBidss 406
Lingula 112,134
LiDgoIepis 112
Liquidambar integrifoliam 323,338
Lomatia inicrophyila 315
f Saportanea 346
LodoviopBis « $90
Lygodiam Dentooi 309
Marvinei .. 309
tricbomanoides 333
Macbairodus 23,25
Mactraalta 35
formosa 35
Magnolia alterDans 355
capellini 356
teuoifolia 355
Ma^oliacesd .- 331
Mulvacead 358
Mastodon 23,25
Araericanus f&i
Megaceratops coloradoenBls '. , 150
Megalomeryx 2>
Megalopteris 279
Melania 22,2:i
MelaniidaD « 391
Melaiupns 22
MeuiHpermites I ^ 331
acerifoHus 3S7
clyclopbyllus 358
obtuBilobuH XS
ovalin 357
SopnlifoliuB 357
alineuBis 357
MerycbippiiB 25
MerycodoB 25
MoliuBca 390
MoreiB 341
Myriea cretacea : 339
inBigntB 312
t LesBiKiana 312
Ludwigii 311
obtasa 339
semiua 340
Negundoides acntifolns 359
NeuropteriB faBcicalataB 279
Noeggeratbia :. 278
OboluB 112
Odoutopteres 281
OlenoB 112
Orbicula 118
Oreodaphne cretacea 343
Oroodon 23,25
Ortbisdesmoplenra 112
Ortboceraa 213
Orthogomopteris 279
Ostrea 20,22,23,136
lugubriB 136
Ottolia ADiericana 300
PalsBOcbsDniB 25
PaleopteriB Boscii 278
Hailiana 2:8
bybeniica 278
JackBoni t 278
obtnsa 279
Roemeri 278
Reusii 278
uniequilateraiis 278
Palinae 338
PaliuruB mombranacenB 360
INDEX OF SYSTEMATIC NAMES. 513
Pago.
Paliuacites Goldianns 311
rimosuB 290
PalcBolagus 25
Pappichthys 158
Paradoxides 112
Patula Cooperi 396
Pecopteris 134
Nebraakaua 333
Pectinibranchiata 390
Persea Lecouteana 343
Sternber^ii 343
Phaseolitesjaglandions i 314
PhitolithuB 281
Phragmi tes oretaceouB 338
Physa 25
heteroBtropha 400
PhysidfB 400
Pbyllites amorpbons 364
betulaefoliiiB 363
rboifolins ; 361
rbomboideas 364
umbonatus 3G4
Yanoufe 364
Pbyllocladns BubiDtegrifoliiis 337
Pinna 134
Pinus Quenstedti 336
Pisidium 22
Pistia corragata 287,289
Mapelii 289
Planera Ungeri 313
PlanorbiDce 402
Planorbis ,. 23,25
PlaBtomenas 154
PlatanesB 341
Platamis-. 23, UU
aceroides 293
diminativa 341
Guillelma 293
Haydeni 32
Heerii 341
NewberriaDa 341
obtasiloba 341
priniera 'Ml
Plenropborus 115
Poebrotberiam 25
Polyoarpicro 355
PomatiopsiDSQ 391
Pompboliginte 405
Populites elegans 339
lancastrieusis 339
PopiiluB 23
arotica 293
melanaria 302
melanarioides 291,302
mutabiliB 291
tremuloides 81,86,93
Potaraoraya 22
PrioiiocycluB WyomingeDsis 136
Procamelas 25
ProduotuB 114,119
aemistriatuB 216,233
BubaoaleatUB 213
ProteacesD 346
Proteoides acuta ' 128,347
dapbnogenoides 347
GreYilleseformiB 347
Protomeryx 26
Protopbyllum crednerioides 363
Ilaydenii 363
33 H
514 INDEX OF SYSTEMATIC NAMES.
Protopbyllum LecoDteanum 363
minaa 3GS
tMudgel 363
maltinerve 36B
TNebraacense 362
qaadratum : 363
ragosam 36S
Stembergii 368
Pnimis americana 949
chickasa 249
tcretaceus 361
pentiillo ..•.^.-. 249
PsyloplutOD S76
Ptenostrobus Nebrasceusis 364
Pteropbj'llam THaydenii 334
Palmouata 391
Pupidflp 391
Papilla alticola : 391
Pupime 391
Quercus alba 86
f Ellaworthiaua 340
furcioervis 203
Hardingeri 313
bezagona «... . 340
Tporanoides 341
Kbamuus 289
rectinervU 291
Rossmaasleri f ^ 314
teuax 360
Rbiuoceros 23»25
Ivbus membranacea 306
Khyncbonella 211
Endlicbi 213
KissoidosB 390
Sabal audegavensis 290
Campbelli 32
commnuis 311
Grayana 289,290,301
l)recur8oria 290
Sageuaria depressa 279
SalixRbeanaT 28S
protesefolia 339
Salvinia attennata 296
Sapiudus affinus 289
DentoDi 315
Sassafras 344
aciitilobum 344
(Aialiopais) cretaceum 344
Tar. deDtatum 344
obtusum 344
mirabile 129,345
recurvata 345
Mudgei 344
Scapbite* 135
WarreDana ^. 136
Selaginella f faloata 297
. laciniata 297
Sequoia acnmiData 310
affinis IflO
biformis 289,290.298
brevifolia— 289,298
condita 335
fastigiata , »3
formosa 33d
langsdorfii 291
longifolia 289,290
Eeichenbacbi , 289,335
rigida 26©
Smitbiaua 289
INDEX OF SYSTEMATIC KAMES. 515
Shepherdia canadenBis 249
Sigillaria 280
Somatogyras eeogouus 390
Sphenopteris 134,278,280
crassa •••.. 280
Hoeninghaiiflii 280
Spirifer 114,115,119,211,216
Spiriferina ,. 115
Steneofiber 25
St6rculia lineariloba 358
Stigmaria 279
fucoides 42,118
SacinineB 399
TaDcredia americana 35
Taxodiam dnbium 293
TerebinthacesB 360
Teetndo 23,24,25
ThaUophytes 333
Tiliaceae 359
Titanotherium 23,25
Todeat Saportanea 322,346
Trapa borealis , 289
microphylla 304
Trionyx 23,24,158
ITlmas 23
Ulodendron minus 280
Unio 22,23
ITnionidso 407
Urticinece 341
Valvata Biucera 390
Valvatidie 390
V'ertiginiDfB ^ 392
Viburnum marginatum 291,306
platanoides 314
rotundifolium 305
Wymperi 306
Vitis lestivalis 249
cardifolia ; 249
Vitriufie 392
Vitrina limpida 394
Pfeifferi 394
Vivipara 22,23,24
trocbiformis 24
Widdringtonia complanata 299
Zamiostrobus f mirabilis 309
Zonaritcs digitatns 333
Zonites conspectus 393
fulvus 393
viridulus » 393
o
TUB I IWll%/eA<»i«%
M ■ SI
THE UNIVERSITY UBRARY
UNIVERSITY OF CAUFORNIA, SANTA CRUZ
SCIENCE UBRARY
This periodical is due on the DATE stamped below.
To renew by phone, call 459-2050
JUL 2 2 199) nn
Series 1665
i ..--
THE UNIVERSITY OF CALIFORNIA UBl
RJ^^
k^-^
tmmm